NOAA Technical Report NMFS Circular 427 

Ocean Variability in 

the U.S. Fishery 

Conservation Zone, 1976 

Julien R. Goulet, Jr. and 

Elizabeth D. Haynes, Editors 

July 1979 

MARMAP 

Contribution No. 146 

(Marine Resources Monitoring, 

Assessment, and Prediction Program) 

U.S. DEPARTMENT OF COMMERCE 

Juanita M. Kreps , Secretary 

National Oceanic and Atmospheric Administration 

Richard A. Frank, Administrator 

Nationai' Marine Fisheries Service 

Terry L. Leitzeli, Assistant Administrator for Fisheries 
The National Marine Fisheries Service (NMFS) does not approve, recommend or endorse any proprietary product or proprietary material 

mentioned in this publication. No reference shall be made to NMFS, or 

to this publication furnished by NMFS, in any advertising or sales promotion which would indicate or imply that N;\IFS approves, recommends 

or endorses any proprietary product or proprietary material mentioned 

herein, or which has as its purpose an intent to cause directly or indirectly 

the advertised product to be used or purchased because of this NMFS 

publication. 
Papers 

1 

2 

3 

4 

5 

6 

7 

8 

9 

10 

11 

12 

13 

14 

15 

16 

17 

18 

19 

20 

21 

22 

CONTENTS 

Introduction. by Julien R. Goulet, Jr. ... ...... ........ .. . ... ........................ 1 

Summary. by Julien R. Goulet, Jr. ................................................. 3 

Atmospheric circulation in 1976. by Elizabeth D. Haynes .......... ..................... . 

Atmospheric climatology and its effect on sea surface temperature - 1976. by Robert R. Dickson 

and Jerome Namias .............................................................. . 

Eastern Pacific sea surface conditions in 1976. by Elizabeth D. Haynes .................... . 

Sea surface conditions in the western North Atlantic in 1976. by Julien R. Goulet and Elizabeth 

D. Haynes ................................................ : .................... . 

Anomalies of monthly mean sea level along the west coasts of North and South America. by Dale 

E. Bretschneider and Douglas R. McLain ............................................. . 

Coastal upwelling off western North America, 1976. by Craig S. Nelson .................... . 

Oceanic conditions during 1976 between San Francisco and Honolulu as observed from ships of 

opportunity. by J. F. T. Saur and Douglas R. McLain .................................. . 

The 1976 El Nino and recent progress in monitoring and prediction. by William H. Quinn ..... . 

Sea surface temperature anomalies. by Douglas R. McLain ............................. . 

Fluctuations of sea surface temperature and density at coastal stations during 1976. by Douglas 

R.McLain .. . ... ............................................................... . 

Data on cold weather conditions along the Atlantic and Gulf coasts during the fall and winter of 

1976-77. by J. Lockwood Chamberlin and Reed S. Armstrong ............................ . 

Wind driven transport Atlantic coast and Gulf of Mexico. by Merton C. Ingham ............. . 

Sea surface temperature distribution from Cape Cod, MA, to Miami, FL, 1976. by Joseph W. 

Deaver III ..................................................................... . 

Water column thermal structure across the shelf and slope southeast of Sandy Hook, NJ, in 1976. 

by Steven K . Cook ............................................................... . 

Anticyclonic Gulf Stream eddies off the northeastern United States during 1976. by David 

Mizenko and J. Lockwood Chamberlin ............................................... . 

River runoff along the middle Atlantic coast in 1976. by Elizabeth D. Haynes ............... . 

Climatic conditions related to the fish kill and anoxia off New Jersey during the summer of 

1976 by Reed S. Armstrong ........................................................ . 

Variations in the position of the Shelf Water front offthe Atlantic coast between Georges Bank 

and Cape Romain in 1976. by John T. Gunn ......................................... . 

Temperature structure on the continental shelf and slope south of New England during 1976. by 

R. Wylie Crist and J. Lockwood Chamberlin .......................................... . 

Continuous plankton records: zooplankton and net phytoplankton in the Mid-Atlantic Bight, 

1976. by Daniel E. Smith and Jack W. Jossi ......................................... . 

Siphonophore ("Lipo") swarming in New England coastal waters-update, 1976. by Carolyn A. 

Rogers ........................................................................ . 

Bottom water temperatures in the Gulf of Maine and on Georges Bank during spring and autumn, 

1976. by Clarence W. Davis . ..... ................................................ . 

iii 

11 

19 

35 

43 

51 

65 

77 

93 

III 

151 

167 

175 

209 

231 

259 

281 

289 

301 

315 

337 

349 

353 
ABSTRACT 

Some responses of fisheries r esou rc e s to 

natural climate-ocean variab i li ty in 1976 

are summarized. Emphasis is on t he U.s . 

Fisheries Conservation Zone . Ar e as in 

which the United States has an e st ab lishe d 

fishery or commercial interes t in a l o ca l 

fishery are also considered . Co ntri b uted 

papers present various aspe cts of the 

marine climate in 1976 . 

IV 
Ocean Variability in 

the U.S. Fishery Conservation Zone, 1976 

INTRODUCTION 

Julien R. Goulet, Jr.! 

Q£g2D Y~ri2~i1il~ in lh~ ~~~~ fi~h~r~ £Qo~~rY§liQo lQO~~ 12ZQ is 

the third vQlume 2 focusing on the effects of natural ocean 

variab ility (jncluding climate scale events) on distribution and 

abundance of fishery resources. The objectives of this series 

are: 

1. to provide resource managers witn an overview and 

assessment of the status of the environment in terms of 

larye area and Long time scaLe naturaL processes and their 

possibLe effects on marine fi~hery resources, and 

2. to provide researchers with an inform~tion source on the 

ocean properties and processes infLuencing fishery 

resources. 

These three volumes have been prepared by the program mana gement 

office of the Marine Resources Monitoring, Assessment, and 

Prediction (MARMAP) 3 program of the Nationa l Marine Fisheries 

Service (NMFS). 

The MARMAP program is a nationaL program of NMFS providing 

information needed for management and allocation of the nation's 

marine fishery resources. The program encompasses the collection 

and analysis of data to provide information on the abundance, 

composition, Location, and condition of the commercial and 

recreati onal marine fishery resources of the United States. 

MARMAP also considers the physical and chemical processes 

influencing fishery resources. 

!Resource Assessment Division, National Marine Fisheries 

Service, NOAA, Washington, DC 2D235. 

2J. R. Goulet, Jr. (compiler), The environment of the United 

States living marine resources - 1974. u.s. Dep. Commer., NO~A, 

NMFS, MARMAP Contrib. 104; J. R. Goulet, Jr. and E. D. Haynes 

(editors), Ocean variability: Effects on u.s. marine fishery 

resources - 1975, U.s. Dep. Commer., ~OAA Tech Rep. NMFS Circ. 

416. 

3For information, contact Chief, Resource Assessment Division, 

NMFS, NOAA, Washington, DC 20235. 

1 
Changes in phys ic a L a nd c hemical p roperties of the ocean 

(currents, temperature, nutr ients, e t c.) and the associated 

moduLation of bioLogicaL process es d ir e ctly or indirectLy affect 

not onLy Lon g -term yields and annual abun dances of fish stocks, 

but aLso their distribution and avaiLab ility. Fishery Oceano-

~raphy , as a subprogram of MARMAP , i ncLudes the analysis of 

physical, chemicaL, and bioLogical ocea nog raphic data coLlected 

durina ~ARM AP and other NMFS surveys and from oceano g raphic and 

meteo~oloa icaL operational and resear c h a ctivities of other 

a~e nci es. ~ Fi~hery Oceanography provided mu ch of the information 

incorporated into Q~~~Q ~~[i~~ilit~ in tn~ ~~~~ Ei~h~[y ~Qn~~[= 

Yg!iQQ IQn~ ~ 12Z6· 

The areas of interest for Q£~2n ~2[i~~ili!y in !hg ~~~~ £i~h~ry 

~QQ~~r~~tiQQ ~Qn~~ l~L~ are the United St a te s ' Fishery Conservation Zone, estabLished by P.L. 94-265 (Fis heries Conservation 

and Management Act of 1976), and the areas of fishery resources 

outside ou r Zone in which we have an estab li s he d fishery or a 

market interest. 

The ~a~ers in this document can be categori z ed as data products, 

event notices, or topicaL summaries. AnaLytic papers, whiLe 

important for understanding the process e s controlling ocean 

variab iLity and conseauent effects on fi s h ery resources, should 

be submitted 10 journals with a broader perspe ctive. PreLiminary 

or summarized research results, ~here ap propriate, may be 

incLuded in tbe pape rs contributed to this s eries. 

The data products, event notices, and top ic a l summaries should 

focus on a limited time interval. The data p roducts should not be 

seLected merely on availability. Rather, pr oducts which portray 

cLimate-ocean prope rties or indices of p rocesses should be 

seLected, or develop ed, for their signific ance to marine fishery 

resources. Topical summaries provide ov e rviews of climate-ocean 

properties and assessment of potential effects on fishery 

resources. The number of these topica l summaries should be 

increased to prese nt more information on p ossibLe environmental 

influences. In future years we hope t o p rovide the summary to 

resource managers in a more timely manner. This may involve a 

smnlL workshop to deveLop the necessary information, and a 

distribution of the summary in draft form prior to distribution 

of the fuLL document as a MARMAP contribut ion. 

We thank our many contributors, who made t his voLume possible. We 

~eLcome criticism, comments, and suggest ions for improvement of 

future volumes in this series. 

2 
SUMMARY 

Julien R. Goulet, Jr. l 

The effects of ocean variability on u.S. marine fishery resources 

can hest be summarized within the conte~t of the broad-scale 

atmospheric and oceanic conditions surrounding our area of 

interest, the u.S. Fishery Conservation Zone. The variability of 

t~e environment within the Zone is controlled by conditions and 

processes in the overlying atmosphere, at the coast, in the open 

ocean beyond our Zone, and along the bottom within our Zone. The 

oapers contributed to this document present a synthesis, not 

necessarily analytic, of the conditions and processes affecting 

the U.S. marine fishery resources during 1976. 

This summary first focuses on the overlying atmosphere, which 

connects the Atlantic and Pacific Oceans across the North 

American continent. The conditions at the u.S. coast, in the 

open ocean beyond our Zone, and along the bottom are summarized 

in turn. Following this, the responses of marine fishery 

resources to the variability of their en vi ronment are estimated. 

Conditions are considered at the 700 mb level, the height of 

approximately the lower third of the atmosphere. This is high 

enough <about 3,000 m above sea level) to be free of surface 

friction, and thus reflects the large-scale conditions and events 

taking place in the atmosphere. It is also low enough to be 

completely within the troposphere, that part of the atmosphere 

which interacts with the ocean. 

Two salient features of the atmosphere in 1976 were the 

continuation of stronger than average westerly winds over the 

Northern Hemisphere oceans and a return to lower latitudes of the 

subpolar low pressure anomaly cells. The variations in westerly 

wind strength and position influence patterns of upwelling and 

offshore wind driven transport as well as sea surface temperature 

distributions. These in turn influence several resource species 

lResource A~sessment Diviiion, National Marine Fisheries 

Service, NOAA, Wasrington, DC 2J235. 

3 
SUMMARY 

such as Atlantic menhaden, Pacific mackerel, a nd Atlantic se a 

herring. The strong westerlie s have pe r s i sted ince 19 71. 

However, the high level pressure patte r ns have unde r~on e drastic 

chan ges in their annual a vera ges ovpr the l as t three years. The 

1976 pressure anomaly patterns at 7 n G mb resemble those o f 1974 

more closely than those of 1~75, but with a few i mro rt an t 

differences. The Siberian high latitude high pressure cell was 

much weaker than in 1974. The subpolar Lew pressure cells wpre 

more intense and covered broader an'as . The r!o rth Ame rican 

continental Lrouqh, Loc ated over the Great Plains in 1974 and 

over the Rocky Mountains in 1975, was over the easte r n seahoa r d 

in 1976. The trouoh indicated a continental w~akenin~ of the 

subtropicaL hiQh ~ressure beLt extEnding aCrOss the Ptlant ic and 

Pacific. That it was over the eastern sea oa r d indicated a west 

coast penetration of Pacific stable hiQh p re ssu re conditions , ana 

consequent Cdlifornia drought. It dlso indicated mo r e unstab Le 

conditions over the eastern seaboard and re ate r precipitation in 

that area. 

The pattern 0f seasonal pressure anorra li es (differences from 

30-yr seasonal averaoes) showed a strikinq change from su~mer to 

falL in 1976. In 1974 and 1975, the annua l avera e anomalips 

were dominated by the winter anomal i es . In 1 76 , t e fdll 

anomaLies were so intense that they dominated the annua l average . 

winter 1975-76, with extremely ~ild past coast conditions , nad a 

zonal distribution of pressure anomaLies <the anomalies tended t o 

line up zonally, or alon? latitUde Lines). The re was essent i a Ll y 

no continental trough, whereas 1974 had a trouoh 0 er the Great 

PLains and 1975 had a deep trough over the Rock i es . Py fall 

1976, the pressure anomaLies rad beco~e meridional (the anoma Lie s 

tended to Line up along meridians), indicating ex tr eme wa v e 

(north-south) conditions in the actuaL pressu r e dist rituti ~ns. 

Extreme wave conditions preceded both the winter of 1917-18 an 

that of 1976-77, the two coldest winters of record in the enster 

United States. 

Haynes (Paper 1) ~resented a summary of atmosphe ric circulatio 

during 1976. Dickson and Namias (Paper 2) d i scussed the interactions between the atmos~here and the sea surface . Summa ries of 

atmospheric conditions over the Pacific (Haynes, Pape r 3) and the 

Atlantic (Goulet and Haynes, Paper 4) aLso p r ese nte d the open 

ocean surface conditions. Chamberlin and Ar~strong (P ape r 11) 

presented statistics on the extreme conditions a lon g the east 

coast in fall 1978 and winter 1977. Quinn (Paper & ) discussed an 

index of the Southern Oscillation, a phenomeno n of the atmosphere 

in the South Pacific associated with the sout~east trade winds. 

This can ce correlated with upwelling along the equator and off 

the coasts of Chile a nd Peru, and with the abunaance of anchoveta 

and tuna in those areas. 

4 
Very little information on coastal conditions was compiled for 

Q£~gD Y~rigQililY in !h~ ~~~~ fi~hg[y £QD~~r~§!iQD IQDgL 12Z~. 

Haynes (Paper 16) summarized river runoff into the Middle 

Atlantic Bight, where the volume flow showed an early spring, 

peaking in February instead of March or April. There also was 

extremelY high flow in October when precipitation in the 

Chesapeake drainage basin exceeded 300% of normal. Precipitation 

exceeded 150% of normal over the entire Appalachian Range in 

October. This extreme precipitation was associated with the 

continental trough and extreme wave conditions in the atmosphere. 

The consequent runoff into the Chesapeake Bay influenced the 

survivaL of oyster spat. 

McLain (Paper 10) summarized fluctuations in temperature and 

density at coastal stations from Maine to Florida, Florida to 

Texas, and ALaska to CaLifornia. The densities at a tide st~tion 

at Kiptopeke Beach , VA, at the mouth of Chesareake Bay, had a 

large negative anomaLy in November, one month Later than the 

extreme fLaw in the Chesapeake. The early onset of the cold 

1976-77 winter was shown by positive density anomaLies in New 

EngLand, a ~onsequence of early freezing and decreased runoff. 

Negative temperature anomalies in fall 1976 extended aLong the 

entire east coast. They began in midsummer south of New Jersey. 

Bretschneider and McLain (Paper 5) summarized historical data 

(1931-75, wi~h some gaps in coverage) showinq variations in sea 

Level aLong the Pacific coast. UnfortunateLy, the 1976 data were 

not available to them. Chan~es in sea leveL over broad ocean 

areas can be reLate d to shifts in wind patterns, upwelling 

regimes, etc., and may be indicative of conditions affectinQ 

certain resource species such as Pacific mackerel. 

The conditions in and beyond the Fishery Conservation Zone were 

summarized by Haynes (Paper 3) and Goulet 0nd Haynes (Paper 4). 

Dickson and Namias (Paper 2) presented a summary and analysis of 

the 1976 conditions . The eastern North Pacific, which began 1976 

with a smaller reserv oir of w~rm surface ~ater than in pre vious 

years, continued to cool. By the end of the year the sea surface 

temperatures were anomalously coLd. Heat storage (average temperature, 0-100 mb) in the Pacific, discussed by Saur (Paper 7) 

also was lower in 1976 than in 1975. 

The centraL Narth Atlantic does not have as strong an influence 

on conditions in the Fishery Conservation Zone as does t~e 

eastern North Pacific. It is downwind of the Zone and is 

isolated from it by 3 strong fr~ntal system, the Gulf Stream. 

5 
The charts of temperature anomaLy (McLain, Paper 9) do not show 

any significant patterns, either positive or negative, in the 

open ocean waters. Ingham (Paper 12) presented maps of Ekman 

transport off the AtLantic coast and in the GuLf of Mexico. In 

1976, the meridional (north-south) component was generaLly more 

negative (more to the south) than the average in the open 

AtLantic. This indicates a stronger westerly wind componen

(stronger zonaLity) than average, which wiLL adversely influence 

survival of certain species such as menhader. 

The bottom does not provide a source of energy or variabiLity i 

time affecting u.s. marine fishery resources. Nevertheless, 1 

shalLower waters at least, the bottom does modify the orocesse 

~ffecting the marine environment. Davis (Paper 22) discussed the 

bottom waters in the Gulf of ~aine and over Georges Eank. Ther 

has been a warming trend since 1968, though it was partiall 

reversed in 1975. In 1976, the spring temperatures in the Gul 

of ~aine and the autumn temperatures, both there and over George 

Bank, resumed their warming trend. This warming in the botto 

waters took pLace despite the coLd autumn air temperatures. I 

may be expected that bottom water temperatures affect th 

recruitment of bottom dwelLing species such as sea scalLops 0 

demersal spawning species such as winter flounder and Atlan t; 

herring. 

Armstrong (Paper 17) discussed the anomaLous bottom anoxi 

conditions leading to a massive fish kiLL off I ew Jersey. Cris 

and ChamberLin (Paper 19) provided a summary of the botto 

temperatures south of New EngLand. ~o information was avaiLabL 

on the broad Bering Sea shelf. 

How did the environment of the U.S. Fishery Conservation Zan 

respond to the surrounding variabLe conditions in 1976: McLain' 

charts of sea surface temperature anomaly (Paper 9) provid 

information on scaLes of one month and 1 00 km, whiLe Dickson an 

Namias (Paper 2) presented an anaLysis on scales of three month 

and 500 km. The change of anomaLies along the Pacific coast fro 

negative at the beginning of the year to positive at the end i 

noticeabLe. These changes paralLel the opposite changes in th 

offshore waters of the eastern North Pacific. The sea surfac 

conditions in the Bering Sea, GuLf of Alaska, GuLf of " Mexico 

South Atlantic Bight, MiddLe AtLantic Bight, and GuLf of Main 

are also charted by McLain and discussed by Haynes (Paper 3) an 

GouLet and Haynes (Paper 4). The temperature anomaLies along th 

Atlantic coast were positive through JuLy and negative for th 

remainder of the year. Fast-swimming fish such as tun 

congregate in areas and dept~s where temperatures suit the; 

6 
prefp.rences. 

species. 

Temperatures affect the growth ra t es of many 

Nelson (Pa~er 6) presented the up ll ng i ndex along the west 

coast from t .he Gulf of Alaska to Ba j a Ca li fornia. The southern 

area had extremely low indices in J anuary-February and from 

September through December. Th e Gulf of Alaska also had 

extremely low indices in April-May, Ju ly through September, and 

in November. The California Curr e n t region had extremely high 

indices throughout t he ye a r exc ept in April and July-August. 

These indices p rovide i nfo rmat ion o n a vailability of nutrients 

brouqht up with upwelled wa t er. Quinn (Paper 8) presented 

indices of the Southern Oscill ation (trade wind relaxation) which 

trackea ~ development of El Nino-type activity in the eastern 

tropi·cal Pacific. Strong El Nino-type activity is detrimental to 

the growth and abundanc e of Peruvian anchoveta. 

The wind driven tran s ports alo n g the east coast and in the Gulf 

of Mexico were discuss ed by Ing ham (Paper 12). In February-March 

the transports were a nom a lously strong to the southeast along the 

u.S. east coast. Du ring November-December, anomalously strong 

southwest trans ports persisted. In the Gulf of Mexico, 

anomalously stron g n orthwest transports persisted from October 

through December. Ons hore wind-driven transport is extremely 

important to £urv i val of Atlantic menhaden larvae. 

Gunn (Pa p er 18 ) ma pped the a n nual march of the Shelf wate r /Slope 

Water front aLon g se ve r a l transects off th e u .S. east coast. The 

front in 1976 was s i9n ific antly more varia bl e than i n 1974 or 

1975. The energet ic st ate of the front mirrored th e energetic 

state (extreme wave pott er ns) of the atmosphere and preceeded the 

cold winter. De a ver ( Paper 13) presented the sea surface 

temperature alon g the ea st coast from Flor i da to Maine. This 

data set, obtained f rom airborne radiation thermometry, reflects 

the early spring and co ld autumn of 19 76. Cook (Paper 14) 

presented the ch ang e s i n water column thermal structure off New 

Jersey. The earl y sprin g of 1976 was also evident in this data 

set. The nears hore surface saliniti~s were much reduced durin g 

spring, and a rel a tively fresh surface layer sometimes extende d 

beyond the Shel f Wa ter/ Slope Water front. (Note the e xtremely 

early sprin g runoff shown by Haynes in Paper 16.) The relativ e 

distributions of Sh el f Wa te r and Slope Water may be important to 

overwinter survival of Atlantic herring larva~. Lowered 

salinities due to h i g h runoff, with associated turbidity, are 

unfavorable to shell fi sh. 

Smith and Jossi (P ap er 20) di s cussed variations in plankton 

populations in the Mi dd l e At l antic Bight by season and water 

mass, and also in a warm cor e Gulf Stream eddy. Named species 

may be considered as water ma s s indicators . Armstrong (P2per 17) 

discussed the anoxic bottom c onditions off New Jersey. This was 
a response to the earLy spring warming, ~ith runoff of fresher, 

Lower density water overLying ocean waters and suppressing mixin~ 

throughout the water coLumn, and the conseouent oxygen depletion 

by biologicaL activity. 

Mizenko and Cbamberlin (Paper 15) presented data on the formation 

of anticycLonic GuLf Stream eddies and their migration through 

the SLope Water south of New England. Eod ies create fast, 

LocaLized cur-rents which can submerge marker buoys and move 

Lobster and crab traps when the eddies impinge upon the upp~r 

continentaL sLope. The totaL number of eddy days wa s reduced in 

1976 compared with 1975, with the summer quarter sho~ing the 

gr e atest red~ction. why the Gulf Stream had a lower energy 

state, as shown by the number of eddies cast off, compared wit~ 

the Shelf Water/Slope water front, is a puzzLe. 

Rogers (Paper 21) provided an update on the swarming of siphono -

p h 0 res i n Ne \oj Eng land co as tal w ate r s • The" lip 0," 0 r s Lim e , 

whic h fouLs fishing nets, was mild in 1976 comrared with 1975. 

What can be said about the response of marine fishery resources 

to t he 1976 status of the environment? We can comment on onLy a 

few fishery resources. These commen~s must be considered only as 

best estimates rather than as definitive statements . 

The 1976 year cLass of 

above-normal upweLling. 

harvest. 

Pacific mackereL was favored by 

This has been reflecteo in the 19 77 

LarvaL menhaden were not favored by the wind-oriven 

transport conditions in the Middle AtLantic 8ight . 

Recovery of the Peruvian anchoveta fishery may be delayed by 

tne mild 1976 EL Nino conditions. 

Anoxia i n bottom ~ater off New Jersey hao littLe effect on 

fi nfish recruitment, aLthough many adults died. ALL age 

g roups of shellfish suffered high mortaLities. 

Decreased Slope Water on Georges Bank favored herring larvae 

survivaL in the faLL. Later survival was adversely influ - enced by the severe winter that folLowed. 

Extreme runoff in October affected crab recruitment in the 

MiddLe Atlantic Bight. The following cold winter also was 

adverse. 

The October runoff was detrimental to survival of the oyster 

spat in Chesapeake Bay. 

8 
Because marine fishery resources integrate the effects of their 

environment through their lifetimes, and because the lifetimes of 

many species are longer than a few years, it is appropriate to 

comment on 1976 responses to prior years' conditions. 

The continued warming of bottom waters in the Gulf of Maine 

may adversely affect the recruitwent of lobster. 

The catch of Atlantic menhaden was up about 30% in 1976 

compared with 1975. The increased catch was not a response 

to increased fishing effort. This fishery was primarily on 

the 1974 and 1975 year classes. These year classes were 

stronger than could have been expected from the wind-driven 

transport in those years. Was the increased catch a 

response to increased abundance caused by some as yet 

unidentified environmental or biological factor? Or was it 

due merely to the increased availability of fish that were 

swimming in denser or shallower schools because of some 

equally unknown influence on their behavior? 

what is the relation between the abundance of summer 

bottom-spawning, short-finned squid and bottom temperatures 

on the o~ter continental shelf and upper slope south of New 

England? The 1975 year class, fished in the fall of 1976, 

was 10 times more abundant than normal. The bottom temperatures were about 1C warmer than nor ma l in late spring and 

early summer. The spawning area of th e short-finned squid 

has not ~een identified, and so the environmental influences 

can not be stu die d • 

What is the connection between the warming of Georges Bank 

bottom ~aters and the reappearance in commerciaL quantities 

of sea scallops there? Sea scaLlo p landings declined 

precipitously in the late sixties. They began increasing in 

1974 and reached their 1965 level in 1976. Bottom 

temperatures in the autumn on Georges Bank fell in the late 

sixties and have gone through an uneven increase since then. 

Because sea scallops are harvested at ages greater than four 

years, a correlation cannot be run between temperat~res and 

landings without obtaining a longer time series of 

temperature and obtaining lagged correLations. Perhaps the 

overaLL warming of Georges Bank bottom waters since 1963 

<about 1.5C) is now heLping recruitment of sea scallops. 

9 
LITERATURE CITED 

BARKLEY, R. A. 

1976. Temperature and dissolved oxygen define skipjack tuna 

habitat. In J. R. Goulet, Jr. (compiler), The environmen

of the United States Living Marine Resources - 1974

p. 10-1--10-2. U.S. Dep. Commer., Natl. Ocean. Atmos

Admin., Natl. Mar. Fish. Ser., ~ARMAP (Mar. Resour. Manit

Asses. Predict. Program) Contrib. 104. 

GOU LET, J. R., Jr., and E. D. HAYNES (editors). 

1 978. Ocean variability: Effects on U.S. 

resources - 1975. U.S. Dep. Cammer., NOAA 

Cire. 416, 350 p. 

10 

marine fishery 

Tech. Rep. NMFS 
Paper 1 

ATMOSPHERIC CIRCULATION IN 1976 1 

Elizabeth D. Haynes 2 

In the North Atlantic, 1976 was characterized by pressure 

patterns near normal in positio n but more intense than usual. 

The winter stDrms were severe, but tracked farther north than 

normaL alLowing mild conditions to penetrate northward. In June 

3n anomalous and persistent high pressure center settled over 

western Europe, creating a severe drought for nearly four months. 

ay October, the ridge progressed to the east and the weather 

returned essentially to normal. At the year's end, winter North 

Atlantic storms harrassed the shipping lanes. 

Surface pressure patterns in the North 

normal in position, on the whole, but 

Air fLow over the area south ~f the Gulf 

than usual untiL the l ast quarter, when 

the U.s. west coast forced surface winds 

clockwise) and become southwesterly. 

ZON, surface conditions approximated 

mean. 

Pacific also were near 

more intense than usual. 

of ALaska was more zonaL 

a persistent ridge along 

to back (rotate counterFarther south, north of 

th e long-term (1948-70) 

In the 

t~ose 

high, 

their 

equatoriaL Pacific, win d and pressure 

of 1972, witn a weakened southeastern 

and Southern Hemisphere storms passing 

usual tracks. 

patterns resembled 

Pacific suotropicaL 

to the north of 

At the 7eG mb Level, winds were much stronger than average alL 

year. ~orthern Hemisphere flow was primarily zonal the first 

quarter, with troughs and ridges beginning to develop in April. 

Deepening continued through the summer, though zonal flow 

persisted over th~ North oacific. A strong blocking rid g e became 

IThis poper is summarized from the AtLantic and Pacific logs in 

19[iQ~[~ ~~~lh~r bQg, Vols. 20 and 21; the weather ana 

circulation articles in ~QQlhly ~gglhgr ~g~i~~' Vols. 1 0 4 ana 

1J5; and cQntributions in the Proceedings of the NO~A CLimate 

Diagnostic Wo~kshop, NOAA , November 4-5, 1976, Washin~ton, DC. 

2Resource Assessment Div iii on, National Marine Fisherie s 

Service, ~OAA, washington, DC 2~235. 

11 
Paper 1 

established over Europe throughout the summer. The pattern 

retrograded in October, with well-developed meridional flow 

continuing through November. The pattern reverted to more zonal 

flow conditions by the end of the year. 

Figures 1.1 and 1.2 show anomalies, or departures, of the 700 mb 

surface from a 30-yr (1941-70) mean height. The annual and 

quarterLy anomalies can be compared to those for 1974 and 1975 

(Goulet and 4aynes 1978). In generaL, sea surface temperatures 

tend to be warmer than normal, and seas calmer, under areas of 

positive height anomaLy, whereas cooler and stormier conditions 

prevail under areas of negative height anomaly. These 

interactions in 1976 are more fully discussed by Dickson and 

Namias in Paper 2. 

JEQ~2_Y - The high and Low pressur e centers over the North 

Atlantic were sLightly closer together and more intense than 

average, bringing record high winds and severe storms to western 

Europe. Posit.ive pressure anomaLies extended over the ocean from 

2JN to 60N. 

In the North Pacific the pressure distributi ons were near normal 

in position put more intense than usual, and storm tracks tended 

to be about 5 degrees north of their average locations. 

Fast mid-latitude westerlies and a three-lob ed wave pattern wit h 

broad troughs characterized the 700 mb circulation, with a strong 

ridge along the u.s. west coast which deflected storms northward 

to Canada ane Alaska. 

£~Q[~§r~ - There were more storms than usual in the Nort h 

Atlantic, and their tracks were far north of normal (the majorit y 

of the storms crossed the coast north of No va Scotia). Surfac e 

pressure was norm2l in outline, but more intense. There was a 

+14 mb cLosed high anomaly over western Russia, and a -17 mb 

anomaLy trough paralleling the west coast of Greenland. 

Pressure was above normal over aLL of the Pacific north of 25N ~ 

with a +75 m height anomaLy at the 700 mb LeveL (+9 mb at the 

surface) in the center of this area. 

The 70C mb wave pattern smoothed this month, with very strong 

westerly winds a few degrees north of normal . These brought near 

record high temperatures over all of the Unit ed States except the 

nor t h w es t corn e r • 

~g[£t - The overaLL pressure pattern on the North AtLantic was 

near normaL but more intense than usuaL with a -18 mb anomaly 

near Iceland and a +11 mb anomaly from 15N to SeN on the central 

ocean. 

12 
· -~-. 

The number of storm centers traversing the North Pacific was far 

above normal. They moved eastward, tracking progressively 

farther north to the Latitude of Seattle, and east of 1bGw 

recurved cyclonicaLLy, with the majority moving toward and over 

the Bering Strait. The ALeutian Low was far to the east of its 

usuaL position. A high pressure ceLL covered most of the eastern 

Pacific south of 45N. 

The 700 mb pattern of fast zonaL flow produced the highest March 

wind speeds since records began. Record breaking warmth 

persisted into March over most of the United States. 

~Qti! - In the North AtLantic, the month was reLatively storm 

free, with storm centers concentrated northwest of a line from 

NewfoundLand to IceLand. A ridge stretched northeastward from 

the Azores higb to SON, 15W, where pressure was nearLy 10 mb 

higher than normaL. 

In the North Pacific there were more, but smaLler and Less 

intense, low pressure storm centers than normal, and they tracked 

more nearLy east than the normal northeasterLy direction. The 

anomaly pattern was weak, with a negative anomaLy trough over the 

ALeutian IsLands associated with the primary concentration of 

storm tracks. 

Fast, 

trough 

PLains, 

west of 

zonaL 70G mb flow persisted across the Pacific, 

developed off the U.S. west coast, a ridge over the 

a trough off the U.S. east coas t, and a pronounced 

Europe. 

but a 

Great 

ridge 

~~~ - Low pressure storm centers formed farther off the U.S. east 

coast and were fewer in number than normal, but followed the 

usuaL storm tracks across the North AtLantic. There was a -12 mb 

anomaLy centered in the IceLandic low, with a Large area of 

miLdly positive anomaLy south of 4SN. 

The number of storms in the North Pacific was near normal, but 

they were more wideLy dispersed than usuaL. The Pacific high and 

ALeutian low remained stronger than normal. 

Mean 700 mb fLow across the North Pacific was fLat and stronger 

than normaL, whiLe waves developed over the continent with a 

trough over the U.s. west coast, a ridge in the western United 

States, and an eastern trough west of the AppaLachians. Mean 

flow over the western North Atlantic flattened and strengthened 

considerably, while an anomalous low developed above the surface 

LQw, and the ridge intensified over Scandinavia. 

J~Q~ - North Atlantic storm paths originated in Ungava Bay, moved 

southeastward to SON, 35~, then recurved toward IceLand. None 

crossed the British IsLes or the Euro~ean continent. A strong 

13 
Paper 1 

ridge north-northeastward from the Azores high brouqht high 

temperatures and drought conditions to northwestern Europe. 

The western North Pacific was dominated by 

pressure celL. The pressu r e gradient 

paths of the storm centers were diffuse . 

a strong surface high 

was very weak, and thp. 

At 700 mb, there was a trough at 175w, and a subtropical ridge 

over the eastern Pacific, which proaressed eastward to bring the 

west coast trough over the western States . Th~re was an 

anomalous strengtheninq of the subtropicaL jet st r eam approaching 

t~e southwestern United States, whiLe pressures rose to the east . 

The trough ~outh of Greenland deepened, and the ri dge ove r 

western Europe strengthened. 

~~ll - The North Atlantic was reLativeLy ouiet, with aiffuse 

cyclone centers. The sea LeveL pressu re pattern was near normaL 

for the month. The few storms that reached =urope did not 

elleviate the drought or ease the recora-breaking heat. 

The Nortr Pacific storm tracks were about 5 deg rees farther south 

and more easterly than normal into the Gu lf of ALaska . There was 

an anomaLous surface low at 55~, 180W, with Lower than normaL 

pressures over the entire eastern North Pac ific. 

The 700 mb flo~ over the Pacific was fast and zonal bpt ween the 

Gulf of Alaska low and a strong subtropicaL high northwest of 

Hawaii. The western U.S. trough retroaradea into the eastern 

Pacific. Ridging over the Great Plains induced a strong trou~ 

over eastern North America. The strong bLocking ridge over 

Euro~e continued, extendin~ southward from a +55 m 700 mb height 

anomaly over the ~orth Sea. 

8~Q~~! - The major North Atlantic storm centers traveLed eastward 

from the Gulf of St. Lawrence, then curved northeasterly and 

passed into the Denmark Strait. The usual sto rm paths south of 

Iceland and across the British Isles were not followed this 

month. Hurricane Belle brought heavy rainfalL tc Long Island and 

southern New England. 

The principal North Pacific storm track was from Japan northeastward into the Bering Sea. The sea level pressure pattern cl ose ly 

matched the climatological mean for the month, although pressures 

were sLightLy Lower (-5 mb) than normal over the ALeut ian chain. 

The 700 mb wind fLow was zonaL between 40N and SeN across the 

entire Pacific Ocean. Troughs Layover bot h coasts of the United 

States, with a ridge over the central States. A deep Low over 

the Davis Strait intensified the drought-producing ridge over 

western Europe. 

14 
~~~l~ffi~~[ - Extratropical storm activity in the North Atlantic 

was less frequent than usual this month because of a stron~ 

(+13 mb anomaly) surface high in this area. One storm, bred in 

the Denmark Strait, brought England 4 inches of rain in 24 hours, 

with winds to 78 ~nots; it was the Woorst in 25 years but did not 

break the drought as the water ran off the dry soil. 

In the Pacific, the surface pressure Nas lower than usual, and 

the high was displaced westward. The Aleutian low was 7 mb 

deeper than normal, sustaining strong westerly winds. Hurricane 

Kathleen, the first tropical cyclone to hit CaLifornia in 

37 years, brought heavy rain to eight western States. Over 

2 inches of rain felL in Death ValLey, and in the San Joaquin and 

Imperial Valleys crop losses were severe. 

The ~ean 7eO mb circulation showed a three-lobed pattern, with 

closed lows over the Alaska Peninsula, Baffin Island, and Franz 

Josef Land. Strong zonal westerLies persisted over the Pacific 

north of 40N. The trough deepened off California and the 

downstream ridge layover the Rockies. The trough over eastern 

North America deepened. The persistent ridge over Europe 

retrograded and a trough became established over Scandinavia and 

the British Isles, extending toward the Azores. 

QflQ~~r - Most of the North AtLantic storms occurred in the 

second half of the w.onth, folLowing the historical tracks from 

the Gulf of St. Lawrence to south of Iceland or from the 

u.S. east coast to northern Europe. The pressure centers were 

near their long-term mean locations, bu t were more intense than 

normal. A trough extended from a -12 mb anomaLy center over 

Land's End southeastward across France. A high north of the 

dlack Sea ridged to a +14 mb anomaly over northern Norway. 

Surface pressure on the North Atlantic west of SOW was within 

1 mb of the climatological mean. 

There were fewer storms than normal in the Gulf of Alaska. They 

originated farther east and south than usual and tracked toward 

British Columbia. The pressure pattern resembled the long-term 

mean, but with a counterclockwise shifting of centers. There was 

a -6 mb anomaly center near SON, 17SW, and a +7 mb anomaLy center 

south of Sitka. 

At 700 mb the Aleutian low persisted over Bristol Bay, but the 

Pacific subtropical high, and consequently the area of strong 

zonal westerLies, retrograded 30 deg of longitude from its 

position of the previous month, and a strong ridge deveLoped over 

Kamchatka. The upper air pattern in this area was tighter than 

normal, end wind flo~ was more intense. The mean trough over the 

eastern Pacific intensified, the ridge over the Rocky Mountains 

persisted, and the trough over the eastern United States 

deepened. A large area of negative height anomaly, with a -127 m 

15 
Paper 1 

center south of Ireland, extended from Italy to the Great Lakes. 

~Q~~~Q~~ - T~e western North Atlantic was rough sailing this 

month. The major storm tracks ran from near Cape Hatteras to 

east of Cape Race and toward Iceland, or else recurved into the 

Labrador Sea. Surface pressure patterns were more intense than 

normaL. The two centers of the Icelandic low were displaced 

southwestward, ~hiLe the Azores high was shifted northeastward. 

There were fewer, but larger than normal, Pacific storms, 

originatins in the Sea of Japan and tracking northeast into thp 

western Bering Sea , or east to the date line then northeast and 

nor h into the Gulf of Alaska. The pressure pattern was much 

deeper than normal with a significant surfac trough extending 

south between 160W and 1SS~ from a -10 mb anomaly over ristol 

Bay. The Pacific high was split into two, with 2 +8 mb anomaly 

over western Montana diminishin to the south-southwest towards 

30N, 135W, ana a +4 m~ anomaly center near 30 , 170E. 

The 70G mb LeveL showed one major trou h parallelino the Asian 

coast and another extending from Dutc Harbor south-southeast 

toward 3CN, 1S0W. The normal ridse over the Rockies was higher 

and sharper than usual, and a trough slo ed southwestward from 

Labrador across the central Unit d States. Flo~ was 

west-southweste rly and more intense than normal over the ~orth 

Atlantic shipping lanes. 

~~£~~~~r - Normal cyclonic activity occurred from tova scotia to 

the Davis Strait and from Newfoundland through the Denmark 

Strait, as well as up the U.S. east coast. Four successive 

storms on this last track battered the srounded oil tanker ~r£Q 

~~rfh~n!' ana the fourth one took the §r~DQ ~~Di!b as well. 

In the Pacific, storms tracked alonq the Aleutian chain into the 

Gulf of ALa&ka. The low was near its usual ~osition, but was 

13 mb deeper than normal. High surface pressure dominated the 

coast south of British Columbia. 

At the 700 mb level, fLow was more nearly zonal than in recent 

months, cut with a ridge over the U.s. west coast, 2 broad trough 

over the east coast, a high over Iceland with an associated fLat 

ridge, and a low over Scandinavia. 

LITERATURE CITED 

GOULET, J. R., Jr. ard E. D. HAYNES (editors). 

1978. Ocean variabiLity: Effects on U.S. marine fishery 

resources - 1975. U.s. Dep. Commer., NOAA Tech. Rep. N~FS 

Circ. 416, 350 p. 

16 
<igure l.l.-Annual mean height anomalies of the 700 mb pressure surface for 1976. Contour interval is 15 m. Hatched shading is <-15 

m; stippled shading is > + 15 m. 

17 
FALL 

Figure 1.2-Quarterly mean height anomalies of the 700 mb pressure surface for 1976. Contour interval 

is 15 m. Hatched shading is < -15 m; stippled shading is > 15 m. 

H1 
Paper 2 

ATMOSPHERIC CLIMATOLOGY AND ITS EFFECT 

ON SEA SURFAC E TEMPERATURE - 1976 

Robert R. Dickson l and Jerome NamiasThe year 1976 saw the continuation of the abnormaLly strong 

westerly fLo~ which has tendec to characterize the circulation 

over much of the Northern Hemisphere for the past five years 

(Namias and Dickson 1976; Dickson and Namias 1978). Ho~ever, it 

is important to note that 1976 aLso saw the apparent cuLmination 

and reversaL of this tendency with a progressive ampLification of 

the circuLation as the year progressed. ~e may crudely summarize 

these changes as follows. A winter of record westerlies at 

relatively high latitudes over the Atlantic and Pacific sectors 

was followed by continue d westerly vigor in spring accompanied by 

a . return of winds and pressure beLts to more normal latitudes. 

Thereafter, ampLification of the fLow progressed throughout the 

Summer as a dominant bLocking ridge built over north~estern 

Europe with shortening of wove lengths upstream, and in fall the 

amplification of the circulation was completed with the 

establishment, on average, of a fuLL latitude 5-wave system in 

the upper westerLies. To some extent, each of these component 

features of the circulation was reflected in the mean annual 

distribution of 700 mb height anomaly for 1976 (Fig. 2.1); ln 

this figure, for example, the welL-deveLoped North Pacific and 

North Atlantic oscillations are clearly shown, as are the 

dominant ridges over the western seaboards of North America ana 

northwest Europe. However, in a year wr.en the key development 

was change itself, a single "mean annual" distribution such as 

this provides a less meaningful illustration of events than do 

the individuaL maps of circulation anomaly for each season. 

These are described in detail below. 

~iQ!~r 1975-76 displ ayed many of the circulation characteristics 

of the preceding season and indeed of the preceding year. As 

shDwn in Figure 2.2, intense suotropical rid£es aominated bot 

M.A.F.F. Fisheries Laboratory, Lowestcft, Suffolk, EngLand. 

2Scripps Institution of Oceanography, La JolLa, CA 92037. 
Paper 2 

the eastern Pacific and north Atlantic, lying well to the north 

of their normal positions and trendinu northeastward to cover 

western North America and the fringes of northwest Europe

Cou~led wit~ intense subpolar lows, on average, over Alaska and 

eastern Greenland, these cells developed polar westerlies o

record intensity over the Western Hemisphere, driving mil 

maritime air into northern North America and Europe, and 

confining arctic air masses to higher latitudes. wagner (1977) 

noted that, in December, liThe 700 mb polar westerlies between 55N 

and 75N over the Western Hemisphere averaged 7.8 mIs, the highes

value since records began in 1943, and as much as 5 mls stronger 

t ~ a n no r mal bet 101 e e n 60 Nan d 65 N • II I nab sol ute t e r m s, the pea 

zonal wino anomaly was developed between southern Greenland an 

Scandinavia where the main jet stream axis was deflected far t 

the north of normal around the Atlantic ridge. In this zone 

upper westerly wind speeds averaged 10-15 mls faster than norma 

in December (Taubensee 1976a). This pattern of vigorous westerl 

circulation over both oceans, Qenerally poleward of normal bu 

periodically expanding south~ard to more usual latitudes

continued throughout the winter. Again, as in previous years" 

the strong westerlies ~ere largely 2 feature of the ocean areas 

ana, with a ~eaker, more meridional flow over the intervening 

continents, the hemispheric wave pattern as a whole was no

without amplitude. Periodically throughout the winter a 

extensive Asian ridge was able to inject arctic air southwaro 

across the western and central Pacific, stimulating intense 

cyclogenesis there and reinvigorating southwesterly flow across 

the eastern Pacific (Taubensee 1976a; Wagner 1976a). Ir 

January, "Wind. speeds across the eastern Pacific and the entire 

Atlantic averaged b to 9 m/s stronger than normal near the 

maximum axis." (wagner 1976a). Meanwhile, with intenSE 

surtropical ridging over both oceans, the subtropical westerlie~ 

(south of 35N) reversed their normal seasonal strengthening treno 

to weaken from December to more than 3 m/s below normal over the 

Western Hemisphere in January (Wagner 1976a). 80th of theSE 

tendencies c~ntinued for the remainder of the winter, wit~ 

temperate westerlies (35~-55N) and subtropical westerlie! 

averaging their second highest and their lowest, respectively 

intensities of record in February (Dickson 3 1976a). Though thE 

situation was somewhat altered in February with the establishmen1 

of troughing at the western American seaboard, the u.s. winter al 

a whole was characterized by intense high latitude westerly flol 

with ridging jn the west bringing drought to the southwest, witl 

frequent chinook winds at the eastern slope of the Rockies, an! 

witb mild maritime air across much of the northern part of th 

country. 

3 No relation to present author. 
r a t-J C I '-

With the continuation of the vigorous westerly regime of previous 

seasons over both oceans, it is perhaps no surprise that the 

antecedent distribution of surface temperature anomaly (Dickson 

and Namias 1978) W8S consolidated rather than destroyed during 

the winter of 1976. The frequent injections of arctic air over 

the west and central North Pacific (with associated cyclogenesis, 

cLoud cover, coLd front activity, and surface water divergenc~) 

combined w;~h high westerly wind speeds to maintain the 

preexisting belt of anomalously cold water across the full width 

of the northern North Pacific (Fig. 2.2). ' In its core area to 

the east of Japan this cold anomaly exceeded 2F (1.1C). To the 

south and east of this coLd zone the eastern Pacific atmospheric 

ridge ext~nding between Hawaii and western North America was able 

to maintain and intensify an area of abnormally warm surface 

water centered on 30N, 150W. Core anomalies here rose by over 1F 

(O.6C) from the previous season to +2.1F (+1.2C). Flanking this 

cell to the eastward, the cool conditions of antecedent seasons 

continued to preveil along the American seaboard. But, with the 

ridge aloft extending well inland, the prime stimulus for the 

earlier cooling (northerLy winds and coastal upwelling) was 

removed. As a result, while still below normal, this coastal 

stri~ warmed considerably from the cold conditions observed in 

the previous fall (Dickson and Namias 19 7 8). At lower latitudes, 

the North Pa~ific cold surface conditions extended westward from 

the coast once more, reflectin~ the northward displacement of the 

eastern Pacific ridge and the resulting weakness of the subtropical midtroposphere westerlies, with attendant strengthening of 

the trade winds at surface level. 

As with the Pacific sector, winter temperatures in the western 

Atlantic were generally cool with an anomaly distribution similar 

to that of the preceding fall. Building on temperatures already 

well below normal, centers of intense cooling developed in the 

Newfoundland area and in the Gulf of Mexico. The former 

reflected the arctic airfLow off the winter continent and the 

record intensity of wind speeds offshore; the severe but 

localized cooling in the GuLf of Mexico [-4F (-2.2C) at the core] 

appears to be at Least partly the result of periodic but intense 

northwesterly fLow from the western ridge which brought arctic 

air and occasionaL record low temperatures to the GuLf coast in 

the early part of the winter. Between these two main centers of 

cooling, a Limited area of warm surface water was maintained off 

the eastern seaboard where the western limb of the Atlantic 

atmospheric ridge supported an anomalous southerly (from the 

~outh) airflQw. The narro~, zonal alignment of this ridge, 

however, meant that this southerly flow and the induced warming 

were necessari ly of Limited LatitudinaL extent. 

Man y e l e men t s 0 f the win t e ,r c i r c u l a t ion W ere m a i n t a i ned i n t a 

~Q!iQg. As shown in Figure 2.3, faster than normal mid-latitude 

westerLies continued to prevaiL in both the Pacific and Atlantic 

21 
Paper 2 

sectors, the product of coupling between intense subpolar lows 

and strong subtropical highs over each ocean. While, on average, 

the low heignt anomaly centers maintainec their winter positions 

over Alaska and southern GreenLand, their corresponding ridges 

moved westward to mid-ocean from tre continental margins and 

returned to more southern latituoes. These movements, coupled 

with a weakening of the AtLantic ridge from +310 ft (+95 m) at 

the 700 mb LeveL in winter to +15 0 ft (+46 m) ln spring, aLong 

with partiaL fiLling of the Greenland Low, effected a generaL 

weakenin g of poLar westerlies and a shift of their main axis to a 

more southern path. Once again, as Wagner (1977) points out, the 

lack of ampLitude in the troughs at mid- Latitudes meant that 

arctic air was LargeLy contained at high Latitudes in spring with 

Little southward penetration over North Ame rica. 

It shouLd be noted, however, that the gene raL westerLy vigor 

impLied in Figure 2.3 conceaLs certain periods of more ampLifieo 

flo~ within the season. The fLow was certainLy fast and zonaL in 

March when ~he temperate westerlies over t~e Western Hemisphere 

attained their highest March vaLue since records began (12.3 mls 

on average; Taubensee 1976b). ~ean anomalies of +5 mls were 

observed at 700 mb aLon q the principal wind axis from the Great 

Lakes to Iceland, with a +12 mls anomaly south of GreenLand. 

However, aLthough vigorous upper westerlies (+9 mls anomaly) 

continued to be generated over the Pacific in April (where 

injections of arctic and subtropical air around the prircipaL 

centers of action were generating a strong baroclinic zone), the 

700 mb circulation ampLified g reatly over North ~merica and the 

Atlantic, and upper wind speeds were slightLy below normal when 

averaged for the western Hemisphere as a whoLe (Wagner 1976b, 

1977). Flat, faster than normal fLow returned, however, to 

characterize both ocean areas for the remainder of the spring. 

In the Pacific sector the continued presence of an intense 

subtropical rjdge Rt higher latitudes than normal, and the strong 

easterly fLow to its south, gave the stimulus for unusuaLly 

strong typhoon activity over the southwest Pacific. 

These deveLop~ents once again were refLected in the distributions of surface temperature anomaLy in spring over the eastern 

Pacific and western AtLantic (Fig. 2.3). With much continuity in 

the tendency of the circuLation from winter to spring, the season 

to season changes in sea surface temperature (SST) anomaLy are 

mainly those of detaiL. The northern Pacific continued to De 

predominantly coLd under its mean trough, aLthough the center of 

cooling [-2.2F (-1.2C) anomaLy in the seasonal mean) was situated 

close to the ALeutians. To the south of this coLd zone an 

expanding beLt of warm surface water marked the clear skies, dry 

settLing air, and oceanic convergence associated with the intense 

subtropical ridge in its new mid-ocean Location. Under its 

eastern fLank, surface warming spread east~aro toward the 

American western seaboard, continuing the erosion of the coLd 

?? 
water fringing the coast. At lower latitudes the strong easterly 

flow around the ridge maintained intense cooling [SST anomaly 

>-2F (>-1.1C)1 westward towards Hawaii. 

Changes in Atlantic surface temperature from winter to spring are 

similarly e~plicable in terms of the movements of both 

subtropical rjdges. The westward movement, on average, of the 

Pacific ridge removed the northerly outbreaks that earlier were 

the source of intense cooling in the Gulf of Mexico. Temperatures there continued below normal, but they increased by over 2F 

(1.1C) from the previous season. The similar westward expansion 

of the AtLantic atmospheric ridge brought the expected 

intensification of warming off the Atlantic states, with 

anomalies exceeding +1F (+0.6C) over a fairly extensive offshore 

area. To the northwest of this ridge, however, vigorous offshore 

westerly flow associated with the upstream trough continued to 

maintain intense cooling off the Canadian Maritimes and Labrador, 

in a continuation of the winter situation. 

While certain elements of the spring circulation were conserved 

into ~~mm~c' the mean distribution of the 700 mb height anomaly 

for summer (Fig. 2.4) was very much more chaotic than before, 

with zonal pressure alignments breaking down into patterns of 

small cells, contributing to a well-amplified mean circulation. 

As shown in figure 2.4, a stronger than normal subtropical ridge 

still extended zonally in mid-Pacific, though its anomalous 

amplitude was halved. As a result, its eastern margin retracted 

westward, away from the American coast. To the north of this 

cell troughing continued ocean-wi de so that the intervening 

westerlies re~ained anomalously strong (+5 to +8 m/s in July; 

wagner 1976c), but the single high latitude trou gh of spring 

split into two weaker isolated cells close to the Arctic coast of 

Siberia and the American North Pacific coasts. 

This continuation of anomalous troughing activity, and strong 

westerly flow at higher latitUdes of the ~orth Pacific, brought a 

further dramatic intensification of cooling in the underlying 

surface waters. with surface temperatures already weLL below 

normal in this zone, the renewed coaling rapidLy lea to the 

development of a vast area of subnormal temperatures throughout 

the western and northern Pacific with core anomalies of -3.5F 

(-1.9C) and -3.1F (-1.7C) underlying the principal centers of 

negative height anomaly to the northeast of Japan and off British 

Columbia. In the southeastern Pacific, equally dramatic changes 

took place. The weakening and westward retraction of the 

subtropicaL ridge meant weaker northerly winds and suppressed 

upwelling off the American seaboard, finally permitting warm 

surface conaitions to extend eastward to the coast. And with the 

coLlapse of tneir parent cell, the weakening of the trade winds 

from their previous strength farther south brought a rapid change 

from cold to warm conditions in the southeastern Pacific, 

23 
t

aper c::. 

contributing to the deveLopment of summer fL ~ino conditions in 

the eastern equatoriaL zone. 

Over the ~orth American and Atlantic s ctors the key development 

was the westward retrogression of the domin nt cent 'rs 0 action 

in summer, with a general shortening of ~dV Len~ hs in the up er 

westerLies and amplification of the mean fLow. From Europe a 

powerfuL preex;stinq bLock moved west~ard to settLe tenaciously 

over Britain and ~ssum~ a dominat;nq roLe 1n the Atl nt;c 

c i r c u l a t ion (F i g. 2. 4). ,~ i t h t his e v nan w i h i n t p n i f i c a -

tion of trouq~ing activity off the pacific Nnrth~ ~t , the we tern 

AtLantic riage was enC0ura .d to move inland to ~dst-c ntral 

North America, Leavinq only a weak su sioiary cell over the 

western AtLant; c. In thE' north tt. pe rsiste t mpan trough over 

Greenland also partici ated in t~is ·ne ral retrogre sion , moving 

westward while retaining its spring intensity, 0 become 

centered, on averaQe, over th Davis St r it. Coupling bet ween 

this cell and the separated centers of ~ositive he;a t anomaly to 

its southwest and s uthe st ;nd~ceu stroro , anomalous 

northwesterly winds from arctic Cana a to t e Laborador Sea and 

vigorous, anomalous s uthwesterly flo at 700 m from sout ern 

Grepnland to Iceland and the r.e qi n -Gr enland Sea . us, 

whilp the circulation i this sector was muc amplified corr area 

to earLier seasons, the pol r westerlies retaine reat vigor in 

the strong baroclinic zone aLone t~e Arctic frin es. In August, 

for example, ~hen the ubpolar trou ana h British rid e ~ere 

both more than three standard ceviat; ns from normal intensity, 

7CG mb level wind speeds were 14 m/s stronger than normaL over 

Icelana tDi CKson, 1976b). 

with the withdrawal of the preexisting ~estern AtLantic ridge to 

North America, the causes of ocean warming off the middle 

AtLantic states and cooLing south of t ewfoundland .ere Dot 

siwultaneousLy removed so that surface temperatures there ecame 

more nearly normal than in former seasons . The strong 

northwesterly component of airfLow from the Canadian arctic was, 

however, responsitLe for maintaining the intense cooling off the 

Labrador coast [anomaly of -3.5F (-1.VC) in the seasonal mean]. 

The events of f~l~ (Fig. 2.5) were apparently of great climatic 

significance, brinqing an end (at least temporarily) to longestablished regimes in the atmospheric circulation and in the 

underLying surface temperature field. Hithe rto, for exampLe, the 

1970's had been characterized by the extreme vigor of the 

temperate we~terlies over both oceans. In fall, however, the 

progressive ampLification of t~e circulation was completed with 

the estabLisnment ot a fuLL train of meridionaL troughs and 

ridges at mid-latitudes of the Northern Hemisphere. While a 

deep, fuLL-latitude trough developed in intensity over the 

centraL North Pacific, the northerly anomaLous circulation along 

its western fLank brought a further increment of cooling to the 

24 
lreaoy chilled surface waters of the northern Pacific, with a 

~ore 5easonal anomaly of -5.3F (-2.9C) developing south of 

amchatka. To the south of this cell, westerlies still continued 

: 0 flow vigorQusly over a restricted sector of the North Pacific, 

Dut the broad coast-to-coast sweep of westerlies--so 

: haracteristic of recent years--was no lenger in operation. 

[ nstead, the anomalous tendency was for strong northward flow in 

[h e eastern Pacific between the mid-Pacific trough and its 

esponse ridge downstream over the American west coast. Already 

?ncouraged perhaps by the preexisting distribution of surface 

emperature anomaly in the easternmost Pacific, which by late 

;ummer had featured a strong nnrthward twist of isotherms and an 

intense anomaLy gradient offshore (Fig. 2.4), this southerly 

airflow was responsible for a further rapid northward extension 

)f warming along the American seaboard, with reduced transfer of 

;ensible and latent heat from the ocean and suppressed coastal 

JPwelling (NeLson, Paper 6). The 1970's thus far had been 

typified by abnormally warm surface temperatures in the east 

Fentral Pacific surrounded by cool conditions eastward around the 

~m erican seaboard. Now, with the cold waters of the northern 

Ja cific becoming encircled to the east by warming at the coast, 

t he SST anomaLy distribution for the eastern Pacific as a whole 

came more closely to resembLe conditions of the 1960's than those 

Df the 1970's just described. 

[n keeping with these developments, the long-established 

co Ld-sea son regime of warm air tempe ra tures in the east of North 

merica and coLd in the west also sh owe d signs of reverting to 

he conditiocs of the 1960's. The pe rsistent ridge over western 

orth America was abLe to direct a chill northerLy airflow over 

he central and eastern states as far as the Gulf and Atlantic 

oasts, bringing extreme lo~ temperatures to all but the western 

ourth of the country. Depressed south of normal by the western 

idge, a vigorous low latitude branch of the jet stream at 200 mb 

bve r northern Mexico and the southern United States activated the 

'u Lf of Mexico storm track earlier in the season than is usual 

wagner 1977), while the establishmen t of a strong baroclinic 

one at t~e Atlantic seaboard c~ntributed to the development of 

intense storms and strong winds offshore (Dickson an d Namias 

976) . As the result of these changes, cold surface conditions 

nee more developed and extended ecross the surface waters of the 

Gulf of Mexico and western Atlantic (Fig. 2.5). 

Finally, Figure 2.6 presents the mean annual distribution of 

SST 4 anomaly (degrees F) over both the North Pacific and North 

Atlantic Oceans in 1976 and provides a good general summary of 

-----

4S ST anomalies for the Atlantic sector were provided by D. R. 

~cLain, Pacific Environmental Group, NMFS, NOAA, Monterey, CA 

93940. 

25 
the dominant events of that year so far as th e oceans were 

concerned. Over both oceans our attention is immediately drawn 

to the record extent of colder than nDrmaL su rfac water; in the 

annual mean, exact ly 90% of the 5 de ree squa r es (20 1 - J ) Ioopre 

below normal temperature in either ocean. In e-ch secto r th~ 

main zone of intense cooLing extended dcross t northern ocean 

areas with the cent~r of coolinq dis Laced to th we st 

reflecting both the antecedent con itio at the cLos f 1975 

and the continuation of the tendency or vigorous westerLy flow 

at high latitudes throughou much f 197b. Farthpr outh , he 

domains uf the strengthened subtropical rio's are md r ed by 

zones of minimum coolino ~r y actual ~-rminq in eac t ocean , 

~.Jhile at stiLL Lower Latitudes, the gene ral st r n th of th rade 

winds flowing around thes p northward-dis Lacec rid e is appa rent 

in the zonClL band of cooling at about 2C'J-25 I . 

These mean annual distributions are thus dominated by the zonal 

circuLation tendencies which characterized t e winter and sp ri 9 

(and antecedent) seasons, rather than y t rro r a~ Lifi d flo. 

which prevaiLed at the cLose of the yeor. ~o . ve r, these latter 

" at y pic a L II con d i t ion s we ret 0 be 0 f m 0 ret an s s; q s i ; i -

cance. With surface temperature ~rodients over he eas e rn 

Pacific in faLL favoring conti~Jed riOQinn 0 er the oc ies , anO 

with the chi lled east favorinc Maintenance 0 t e east coast 

trough, the stage was set for the intensi ica io of he fall 

temperature regime into the recQrd brea'i 9 .. inter conditions of 

1 977. 

ACKNO\>;L DGt"IE TS 

Part of this research was sponsored by tr.e t ati nal Science 

Foundation, Office for the International ~ecaGe of cean 

ExpLoration, under NSF Contract No. OCE74-24592 , ano the 

University of California, Sa~ Diego, Scripps Institution of 

Oceanography, through NORPAX. 

LITERATURE CITED 

DICKSON, R. R. 

1976a. weather and circuLation of February 1976. Extrem 

warmth over the eastern two-thirds of the United States. 

weather ~ev. 104:660-665 . 

1976b. weather and circuLation of August 1976. 

wetness in the West and dryness in the ~;d~est. 

Rev. 104:1455-1460. 

26 

Extremes 0 

·; o. \oIeathe 
idper 

-

DICKSON, R. R., and J. NAMIAS. 

1976. North American influences on the circulation and 

climate of the North Atlantic sector. Mo. weather Rev. 

1 04 : 125 5-1 265. 

1978. Atmospheric climatology and its effect on sea surface 

temperature - 1975. In J. R. Goulet, Jr. and E. D. Haynes 

(editors), Ocean variability: Effects on u.s. marine . fishery resources - 1975, p. 89-101. u.s. Dep. Commer., 

NOAA Tech. Rep. NMFS Circ. 416. 

NAMIAS, J., and R. R. DICKSON. 

1976. Atmospheric climatology and its effect on sea surface 

temperature - 1974. In J. R. Goulet, Jr. (compiler), The 

environment of the United States living marine 

resource~ - 1974, p. 3-1--3-17. u.S. Dep. Commer., Natl. 

Oceanic Atmos. Admin., Natl. Mar. Fish. Serv., MARMAP (Mar. 

Resour. Monit. Assess. Predict. Program) Contrib. 104. 

TAUBENSEE, R. E. 

1976a. Weather and circulation of December 1975. A warm 

month across much of the country. r.o. Weather Rev. 104: 

325-330. 

1976b. weather and circulation of March 1976. 

precipitation around the Great Lakes. 

104: 809 -814. 

WAGNER, A. J. 

Record heavy 

Mo. Weather Rev. 

1976a. Weather and circulation of Ja n uary 1976. Increasing 

drought in California and the southern Great Plains. Mo. 

Weather Rev. 104:491-498. 

1976b. Weather and circulation of April 1976. Unprecedented spring heat wave in the northedst and record drought 

in the southeast. Mo. Weather Rev. 104:975-982. 

1976c. Weather and circulation of July 1976. Wet in the 

southwest but continued drought in the northern p l ains. Mo. 

Weather ~ev. 104:1333-1340. 

1977. The circulation and weather of 1976. 

23-47. 

27 

Weatherwise 3 '-'· u • 
'\ 

-b 

"' - ... I 

1 

... 

j 

/ 

/ 

\ 

" . 

.(> 

" 

}--

, 

~ 

!' 21040 

I '2 ~ 

, 

J~ 

1976 MEAN ANNUAL 700 mb HEIGHT a ITS ANOMALY (feet+IO) 

Figure 2.1.-Mean annual height of 700 mb pressure surface and its anomaly (departure from the long-term. 194 -72. mean) in ft no. 

28 
700mb HTOM 

I 

I 

/ ,~ 

SSTOM 

Figure 2.2.-Anomaly (departure from the seasonal mean;' base 1947-66) of 700 mb height for winter (December 1975-February 1976) in 

ft/l0 (upper), and anomaly of sea surface temperature for winter in degrees F (lower). Anomalies > + IF are stippled, > -IF are 

hatchoo. 

29 
. Ii> " ,/ 

~ 110 

6. ~"" rO::O ". ft;/3- ~ v 

'>I» ~ 

'i!;io .... i--- . ( bf 4i 

"'-... ft 'm: ~ I . os: 

. 

tIT 700mb HTDM 

SSTDM 

Figure 2.3.-Anomaly (departure from the seasonal mean) of 700 mb height for spring (March-May 1976) in ft/ IO (upper), and anomaly 

of sea surface temperature for spring in degrees F (lower). Anomalies >+ IF are stippled, >-IF are hatched. 

~o 
SUMMER 1976 , - ~~~"~I~~~ --'-----'-

700 mb HTOM 

SSTDM 

Figure 2.4.-Anoma ly (depa rture from the seasonal mean) of 700 mb height for summer (June-August 1976) in ft/ l0 (upper), and 

a nomaly of sea surface temperature for summer in degrees F (lower). Anomalies >+ IF are stippled, >-IF are hatched. 

31 
..... 

, ' 

" , 

, .J. 

?n , Iil 

} +7 

-9 ,., 

". 

)( 

)( 

" ,0 

.j, 

x 

'~ , 'a Iq, 

"0 

~ -l>. ., 

';!i; ~ oj\ 

, " 

'.b. ~ II! 

I,s. 1<! 

1 .,., ... ... " . '" 700mb HTOM 

SSTDM 

Figure 2.5.-Anomaly (departure from the seasonal mean) of 700 mb height for fall (September-November 1976) in ft/IO (upper), and 

anomally of sea surface temperature for fall in degrees F (lower). Anomalies > + IF are stippled, > - IF are hatched. 

32 
SSTDM 1976 

~ /' 

,. \ 

/' <~ 

/~~ /' 

,~ 

(i1. 

/ 

. / 

/'~ 

Figure 2.6-Mean annual anomaly from the long-term, 1948-67, mean of sea surface temperature in degrees F for the :-Oorth Pacific Ocean 

(upper) and the North Atlantic Ocean (lower). Anomalies> + IF are stippled, > -IF are hatched. 

33 
SPRING 1976 . -" 

., 

" ". 

i' 

of' ,0 ~ 

,~ 

.... } '("~\ t '" ~ 

J,;;--t--V"~~~ ,; 

I , , . --ry y ;t ~ 

"0 

(. .... 'fi 

~ 

... ., . 

700 mb HTDM 

-..,... ~-l--+ 

SSTDM 

Figure 2.3.-Anomaly (departure from the seasonal mean) of 700 mb height for spring (March-May 1976) in ft/ lO (upper), and anomaly 

of sea surface temperature for spring in degrees F (lower). Anomalies >+ IF are stippled, >-IF are hatched. 

30 
SUMMER 1976 ~ ~=~~~~--.-----~ 

' 0 

ffO 

700 mb HTDM 

.~ 

~ 

.·~ .~ / " . 

.j, 

'>b 

' 0 

SSTDM 

Figure 2.4.- Anomaly (departure from the seasonal mean) of 700 mb height for summer (June-August 1976) in ft/ IO (upper), and 

anomaly of sea surface temperature for summer in degrees F (lower). Anomalies > + IF are stippled, > - IF are hatched. 

31 
700mb HTDM 

SSTDM 

Figure 2.5.-Anomaly (departure from the seasonal mean) of 700 mb height for fall (September-November 1976) in ft/lO (upper), and 

anomally of sea surface temperature for fall in degrees F (lower). Anomalies> + IF are stippled, > - IF are hatched. 

32 
" 

,/ '0 

~ /- '", 

'~ / 

'-tl 

~\ I 

,- t , 

~ ... 

I 

"Ii 

SSTDM 

','0 7 

f - ' 

i 

--, IW , ... 

t 2<>-- ~ 

lao I 

170 

+ I 

~ 

j ~ 

1976 

: ... ~ ,'f' 

,60 

\ 

~ - ,., ,05 ~ , 'IS' --'- r ,or .... 

. x.... ., f I r"' II , ~ . - i" ~ 

'i , ,/ , * ~ l1 I 

+- '~\ f, _,I' i-' \ --:\-' ~ ~ ,v -, .... \ f> $ ~.' . ), 

.\ 'if} \ _0 

-' ..t;.-M-" iii 

/ .. ) , >v ,., 

~\\ < .. f> \ 

, +.- -4' 

Figur e 2.6-l\lean annual anomaly from the long-term. 19.j~-n7, mean of sea surfa ce temperature in degr r ~ r th rth Po IIi 

(upper) and the :'Iiorth Atlantic Ocean (lower). Anomalies > + I F a re ,tippled. IF are halchl'd. 

'3 

I 

n 
Paper 3 

EASTERN PACIFIC SEA SURFACE CONDITIONS IN 1976 1 

ELizabeth D. Haynes 2 

he annuaL average sea surface temperature ( SST) over the entire 

~astern North Pacific (ENP) 3 north of 30N was colder than normal 

y about 1C in 1976. (ALL comparisons are to the 20-yr mean, 

948-67.) An anomalous warm patch along 30N centered at about 

f50~ persisted until early faLL. This warm patch was associated 

ith the circuLation around the North Pacific subtropicaL high. 

Cold anomaly water lay to the south of ZON during this time. In 

September the anomaLy pattern began to rotate counterclockwise. 

his occurred as the surface pressure pattern also rotated, the 

igh center becoming displaced to the northeast and the Aleutian 

low center far to the west of their normal positions. Throughout 

~he year the winds were stronger than average. In generaL, 

surface winds north of 4GN and south of Alaska tended to be more 

ijesterly thao normal until September, then they became more 

southerly as Lhe Aleutian low retreated westward and deepened, 

ringing unusual warmth to the North American coast and cold to 

he west of 145W and across tD Asia. 

ff southern California a warm patch developed in early summer 

(both warmer than the 20-yr mean and warmer than in 1975) and 

g rew for the remainder of the year. The sea surface was much 

armer than usual along the entire coast during the last quarter. 

The eastern tropical 

a t the beginning of 

appeared near South 

advanced. . By June 

Pacific (ETP) 4 was much colder than normal 

the year. Small patches of warm SST anomaly 

America and beca~e larger as the year 

the anomalously warm waters dominated the 

IThis paper is summarized from £i~hiQ~ lQiQrm~tiQQ' 1Y76, 

Southwest Fisheries Center, NMFS, NOAA, La Jolla, CA 92038; the 

we~ther and circulation articles in ~~Qlhit ~~21h~r R~~i~~' Vols. 

104 and 105, and the Pacific logs in ~2riQ~r~ ~~21b~r bQg, 

Vols. 20 and 21. ~Resource Assessment Division, National 

Service, NOAA, washington, DC 20235. 

3ENP = ZeN to the Aleutians; North American 

4ETP = ZGS to 30N, American coast to 18uW. 

35 

Marine Fisheries 

coast to 180W. 
~aper ~ 

equatorial areas east of 12 Gw, and continued to spread for the 

remainder of the year. 

The ocean-atmosphe re circulation patterns and the warm SST ~ 

durinq the second half of 1975 resembled those of 1972, a major 

El Nino year. The anchoveta fishery was not affected during the 

first half, but later on the catches were not good north 01 

callao; the anchoveta were t~o small. Tuna fishing also wa~ 

poor near Ecuador from May to November, but improved in December 

South of 15S, though, fishing was not affected by the warm water! 

to the north. The normal counterclock wise high pressurE 

circulation with its associated southeast trade winds wa~ 

weakened by frequent storm passages farther north than usua 

auring the Southern Hemisphere winter. In general, the surfacl 

pressure gradient southwe5t of Peru was flatter than usual fOI 

this time of year. Because SST's remained above normal througl 

December over mast of the ETP, 1976 should be classified as an E

Nino year . However, by the last ~eek of the year there wer 

indications that the El Nino conditions were dissipating. 

4gQ~~r~ - Eastern North Pacific sea surface temperatures dropp e

seasonalLy O.6C-2.2C from December 1975. The SST anomaly patterl 

was similar to that which persisted throughout 1975, with a ~ar!

(+1C anomaly) pooL centered about 30N, 150W in the central ENP 

and cool (-1C anomaly) water 100 km out alL along the Nort 

American shore to 3CN, and westward south of that latitude 

Strong surface pressure gradients betNeen the deep Aleutian lOI 

and a strong ridge off the u.S. west coast caused strong sout 

to southwest winds north of 30N ~nd east of 165w to 135w. Storm ~ 

tracking south of the Aleutian Islands were more intense tha 

usuaL, and by increased mixing may be responsible for increasin 

the negative SST anomaly in this area. 

Exce~t for smalL isolated patches, the ETP was significantl 

cooler than normal, reaching -3.3C anomaly at 15N, 95W of 

Guatemala and at 7N, 93W. Temperatures over the tuna fishin 

grounds soutb of 2JN and east of 110W were mostly below normal 

and the fishing fleet was widely scattered. The extensive area 

of negative SST anomalies were associated with strong an 

persistent northerly winds. Off south ern 2aja Californi 

temperatures were slightly above normal and fishermen made goo 

catches in this area. 

Off Ecuador the equatorial ocean front began to weaken toward th 

end of the month. Sliqhtly positive SS T anomalies occurred of 

the Gulf of Guayaquil. Tuna fishing was exceptionally good i 

this area. 

£~Qr~2r~ - Seasonal cooling of the ENP occurred at a near norma 

rate, with temperatu res dropping up to 1C from January values 

except off California and Baja California where SST's ros 

36 
sLightLy. The anomaLy oattern cLoseLy resembLed that of January, 

aLthough the area of positive anomaLy contracted and moved 

northward sLightLy and the area of anomaLy greater than -1C aLso 

decreased. BeLow normaL temperatures continued off the North 

American west coast. 

ALong the western boundary of the PerJ Current, SST's increased 

1C to 2C since Last month from SN to 20S between 8SW and 11SW. 

Warm anomaLies of up to +3C occurred inshore of this area. This 

above normaL warming was ass0ciate d with a Southern Hemisphere 

high pressure system which was weaker than usuaL. The equatorial 

front between oSW and 9SW was very weak. SST's in this area 

exceeded 2bC and the fleet mede exceptionalLy sood catches of 

yeLlowfin tuna. 

During this month northerly winds from the Gulf of Mexico 

frequently penetrated the Gulf of Tehuantepec and the Costa Rican 

fishing grounds. Strong winds and rough seas caused very bad 

fishing weather up to SCC miles south and west of these areas. 

SST's were lowered as much as 3C by wind mixing. The Gulf of 

Panama also experienced extensive wind mixing of surface Layers 

and beLow normal surface temperatures. 

A severe earthquake occurred in GuatemaLa on 4 February. At 

0930 GMT that day, at 14N24', 94W2S', the ship YQigy~ EQr!yo~ 

reported, "Ves.sel suddenLy jumped twice, shuddered vioLently in 

caLm sea." 

~~r~n - Seasonal cooLing continued over the ENP; SST's dropped 

up to 1C since last month and approached the annuaL minimum. The 

anomaLy pattern continued siffiilar to last ~onth·s except that the 

-1C anomaLy pool centered at 25N, 135W in February disappeared. 

winds associated ~ith low pressures in the Gulf of Alaska were 

stronger than normal. 

In the ETP sea surface warming is expected in March. However, 

the fishing grounds southwest of baja California experienced 

cooLing greater than 1C, and fishing decreased due to rough 

weather. Most of the fLeet shifted to south of 2 DN where the 

SST's were up to 1C above normal. 

Tuna fishing was very good south of the Gal~pagos Islands where 

SST anomalies. were positive. Above normaL warming occurred o f f 

Ecuador and offshore of Peru, the +1C anomaly areas showin g u~ 

cLearly in NESS sateLlite charts from infrared data and from shi p 

reports. South of 10S and east of 78w, SST·s have been up to 1C 

beLGlw normaL along the coast of Chi Le for many mo nths. 

~Qrii - Sea surface temperatures over most of the EN P increase d 

ohLy sLightLy from the March minimum vaLues, and d r op pe d up to 

O.6C between aaja CaLifornia and Hawaii , cr e ating a large area of 

37 
-1C ano maly water. Anomalies of -1C showed also south of the 

Aleu t i an s and off the coast of Oregon. A strong surface pressure 

gradi ent north of 40N ca u sed s tro ng er than normal westerly winds 

which contribut e d t o the below normal heatin g in this area. 

There were l ar g e a r ea s of u p t o - 2C a no ma ly water centered at 

10N, 100W and at 1 ON, 14CW . In c oth areas, above normal 

northeast t r ad.e wind s and cl oud c ov er persisted most of the 

month, leading to more v e rtical mix i ng and le s s heat i ng t h a r 

usual for Apri.l. Th er e were much s ma ll er areas of up to +3C 

anomaly \oj at e r west of Gu ay aQu i l to 90 \~ • 

Along the equator east of 120w, upwelling was diminished and thE 

surface was warmed by solar heati n g in very light wine 

conditions. South of 10S along the CDas t of Peru, upwelling ir 

the P~ru Current maintained below normal SST's during the month. 

~~t - Sea surface temperatures increased a t a below normal ratE 

over the entire ENP this month. Greate s t ~arming, up to 1.7CI 

occurred off the coasts of washington an d Ore gon out to 40 0 mile~ 

offshore. The SST anomaly pettern was similar to that of thE 

previous month, but the area of warm anomaly decreased somewha1 

and the area of >-2C cold anomaly increa s ed si g nificantly. 

There was a strong surface high pressu re cell centered neal 

35N, 14SW and a deeper than normal Aleut ian low, causing stron ~ 

winds; the nQrthwesterly winds west of th e low contributed t( 

lowering the SST's southeast of the Alaskan Peninsula, whilE 

southerly winds east of the low warmed the surface off thE 

Pacific Northwest. 

Extensive ~arming occurred along the e qu a tor east of 11Sw, 

Positive SST anomalies were >+2C in f ou r areas where upwellin! 

was weaker than normal. The warm offshore wa ter moved closer t c 

the coast of Peru from the equator to 10S than in any month sinCE 

December 1972 when El Nino reached its ma x imum intensity. Thl 

normal surface high pressure center off the coast of Chile an( 

Peru was weakened this month by the pass a ge of frequent storms. 

In the fishing grounos north of the e quator, SST's increase( 

faster than normal. In the area east of 11 0W, the large negativl 

anomaLies of March decreased to near norma l this month. 

4~D~ - Sea surface t~mperatures increased by up to 4.4C over thl 

entire ENP due to seasonal warming. Th e areas of >-1C anomal) 

decreased greatly, and a smalL patch of >+1 C anomaLy appeared of1 

southern CaLifornia. Between 30N to 4SN and 140~ to 170W, 

temperatures that were up to 1.7C belo w normal last montl 

increased to above n~rmal vaLues due to decreased cLoud cove, (i~creased solar radiation) and Lighter win ds (decreased laten1 

and sensibLe beat flow from ocean to at mosphe re). CoLd anomaLie~ 

38 
decreased aLso in the GuLf of ALaska. A strong surface hiQh 

pressure area occupied the entire ENP, bringing strong 

northwesterly winds from Vancouver Island to central California. 

In the ETP, east of 120W, SST's increased at above normal rates 

north of the equator and increased markedly in the Southern 

Hemisphere. The SST's were higher here than in any June since 

1Y72, a major El Nino year. The positive SST anomalies from 10N 

to 10S, east of 120W to the coast and south to below Pisco, Peru, 

were larger than those of June 1965, an El Nino year. There was 

a marked reduction of low stratus, because of the decreased 

3ir-sea te~rerature contrast, and an increase in cumuliform cloud 

clusters, with low barometric pressures, frequent frontal 

passages, and disruption in the southeast trade winds in this 

area usuaLly dominated by the southeastern Pacific high. 

Tuna fishing off Ecuador decreased sharpLy as the water 

temperature rose. In the Northern Hemisphere tuna fishing was 

very Jood, especially on the ALbatross PLateau and northwestward 

after Hurricane Annette moved through early in the month. West 

of 120W tuna fishing was better than usual in water slightly 

warmer than normal with light winds and seas. 

~~ly - Seasonal warming caused SST's to increase over the entire 

ENP. The warm anomaly pool in the central ENP moved 20 deg 

southward, apd a small warm patch appeared off Oregon due to 

decreased northerly winds and less intense upwelling. 

Sea Level pre&sures were up to 7 mb l~ er than normaL over the 

entire ENP. Strong surface pressure gradients caused above 

normal westerLy winds, resulting in increased evaporative and 

conductive cooLing and vertical mixing. A large area of anomaLy 

>-2C appeared along the 45th parallel and into the Gulf of 

Alaska. 

ALong the equator the SST's showed a tremendous area of anomaLous 

warming, especially east of 12QW. NormaLly the temperatures in 

July decrease 1C or more in this area. Warming appeared in the 

Peru Current, typifying an El Nino year. Below normal surface 

~ressures and surface winds south of the equator to 20S and east 

of 110W were associated with an unusuaLly weak subtropicaL high 

pressure center off South America. Low pressure centers and 

fronts frequently passed eastward through this area which 

normaLly is dominated by high pressure, weakening the southeast 

trade winds here. 

Southwest of Baja CaLifornia the tuna catch was good in waters 

warmer than normaL. 

39 
Auoust - Except for a small patch off northern California , the 

~~ti~~ ENP north of 3SN was anomalously cold, up to -3.SC in 

spots near 4SN, 17SW. SST ·s increased during the month, but at 

below normal rates. A band of s li ght ly (OC-1C) warmer than 

normal water persisted across the ETP from 2S N to 3SN except nea r 

Baja CaLifornia where upweLLing increased due to northwesterly 

winds. 

Sea level pre&sures were near 

slightly stronger gradient' 

winds north of 40N. 

normal in pa ttern but with a 

resulting in above normal westerly 

The equatorial band of warm SST anomalies r eached +4.SC and 

extended souLh alonq the coast to belo w Pi sco , Peru. The 

subtropical high pressure center was displaced , and the sou theast 

trades were interrupted by passinq stormS . Toward the end of the 

month the normal high pressure pattern became reestablished. 

Six tropical deprossions formed in the area from 10 J to 1S and 

100W to 120W where SST·s were above 29C. Two of these developed 

into hurricanes which moved through the fishing g r ounds south of 

the Revillagigedo IsLands. Southwpst of the sto r ms ' paths winds 

and seas were unusualLy liQht where the southeast trade winds 

were interrupted, and tuna fishing ~as exceptiona lly good . The 

heavy cloud cover associated with the storms created sma ll areas 

of negative SST anomaly. 

~~Qt~mQ~[ - Sea surface temperatures in the ENP decreased 

seasonally by O.SC to 1.7C over ",ost of the Gu lf of .ALaska and 

down the west coast to southern CaLifornia . SmaL L increases 

occurred over a large area between Saja CaLifo rnia and Ha waii. 

The anomaLously cold area spread southward to 33~ , but a patch of 

+1C anomaLy appeared at 23N, 12SW. Sea level pressures were up 

to 8 mb beLow normal with a stronc ALeutian Low pressure syste~ 

and strong westerLy winds. 

In the ETP the arp.a of warm anomaly increased greatly, centered 

on about SS and extending from offshore of Ecuador and Peru to 

1S0W. Alt~ough the low level atmospheric circulation returned to 

normal early in the month and the southeast trade winds became 

reestabLished, a succession of low pressure centers moved across 

the southe~sL Pacific at lower Latitudes than usual Later in the 

month and again disrupted the normal wind flow along the coast 

from the equator to 1SS. There was only a very small area of 

upweLLing immediateLy offshore of Guayaqui l and some south of 

Pisco. 

Four tropical storms formed over the waters warmer than 29C south 

of Mexico ana moved northwestward, one doing considerabLe damage 

in southern California. 

40 
Q'!Qb~r - A large and intense lbw pressure system settled over 

Bristol Bay this month, bringing storms with unusually high winds 

and severe weather. Wind mixing of the ocean surface layer 

caused SST'£ to drop at t~ice the normal seasonal rates 

throughout the ENP west of 13~W and north of 3QN. South of a 

Line southwestward from San Francisco and east to the coast, 

above normal SST's were associated ~ith persistent surface high 

pressure, light cloud cover, and Low ~inds. 

Positive SST anomalies covered almost the entire ~TP. North of 

10S and east of 135W SST's were significantly above normal. 

Light winds and warm seas aided fishermen in this area. The area 

of above normal temperatures in the ETP was greater than in any 

month since January 1973, which marked the end of the 1972 El 

Nino condition. 

Three small areas of negative anomaly occurred off Chala and 

Lobitos, Peru, and at 8N, 97W. Above normal winds and extensive 

cloud cover associated with weather fronts moving through this 

area kept the surface layers well mixed, ana upwelLing was active 

south of 15S along the coast. 

~Q~~mQ~r - Seasonal cooLing was weaker than normaL over most ot 

the ENP. Cold anomalies receded slightLy along the u.S. and 

Canadian coasts under the influence of an anomalous high over the 

Northwestern States and its associated light southerly winds and 

clear skies. A deep Bnd persistent low over t he Aleutian chain 

at 165W caused strong winds and rough sea s. It dominated weather 

co~ditions across the entire western Paci fi c north of 35N and 

brought anomalous cooling to the Hawalian IsLands. 

Seasonal warming progressed along the coast of South America 

under Less than normal cloud cover. Anomalously warm seas 

prevai led offshore 10 deg north and south of the equator to 180W 

and beyond. In the Gulf of Tehauntepec SST's were 1C to 2C below 

normal as the result of strong northerly winds and cold outbreaks 

which carriea across from the GuLf of Mexico. 

~~£~mQ~[ - Sea surface cooling of the ENP proceeded at less than 

the normal rate, thus diminishing the area of negative SST 

anomaly. NorLh of 30N, surface winds were more southerly than 

normal, blocked to the east by a high pressure ridge off the 

northwestern u.S. coast. 

The Aleutian low was much deeper (-13 mb anomaly) 

and slightly southeast of its usuaL position. 

associated wiLh this low caused considerable ocean 

beLow normal SST's prevailed west of 15CW. 

41 

than normal, 

Storminess 

mixing, and 
Paper 3 

The ETP continued anomalou ly 

upwelling alonqside the COIS 

that of the two recent El N no 

slightly more extensive than n D C 

in December 1972. The sub ropicil 

frequently weakened by pass n~ ea her 

and surface winds over the ETP 

42 
Paper 4 

SEA SURFACE CONDITIONS IN THE WESTERN NORTH ATLANTIC IN 1976 1 

Julien R. Goulet, Jr. and Elizabeth D. Haynes 2 

This summary essentially is limited to the area off the U.S. east 

coast from florida to Nova Scotia and about 1,000 km offs~ore. 

The Gulf of Mexico is mentioned briefly also. 

In general, the sea surface off the eastern seaboard was warmer 

f han usuaL through JuLy, then tended to be sLightLy cooLer than 

average. In January, there was cooLer than normaL water 

mmediateLY surrounding Cape Hatteras, but this was soon 

is~eLLed by warm air and mixing during the warmest February in a 

entury. This warmth continued through the spring. As the 

ummer advanced the sea surface warmed seasonaLLy, but at a lower 

te than usuaL, so that the warm anomalies became smalLer until 

in August the sea surface was c~oLer than normal in the Middle 

tLantic Right and essentiaLly avera~e elsewhere except south of 

ova Scotia where warm anomalies persisted through the year. The 

eather was mild untiL late in the y ea r, as storms tracked far 

ro rth of normaL. Very few crossed the coast south of 

ewfoundland until Qctober. There were several severe storms up 

t he U.S. east coast during the last quarter. 

Except for Maine and Florida, the entire country was warmer than 

normal during the winter of 1975-76 (December-February). Warm 

co nditions continued through spring, alt hough not quite so 

markedLy. Summer was cool aLmost everywhere except Maine, which 

r emained warmer than usual. Autumn (September-November) was 

.I Th is paper is summarized from g~li~ir~2m' Vol. II; the 

AtLantic Logs in ~2riQ~r~ ~~2!h~r bQg, Vols. 2Q and 21; the 

we?ther and circulation articles in ~~Qlh~~ ~~21h~r R~~i~~' 

VoLs. 104 and 105; Gulf Stream analysis charts, Environmental 

Products Group, NESS, ~OAA, Washington, DC 20033; temperature 

a nomaLy charts, Pacific Environmental Group, NMFS, NOAA, 

Monterey, CA 93940 (see McLain, Paper 9); airborne radiation 

thermometer charts, Coast Guard Oceanographic Unit, Washington, 

DC 20590 (see Deaver, Paper 13). 

2Resource Assessment Diviiion, National Marine Fisheries 

Service, ~OAAI Washington, DC 20235. 

43 
P a ~e r 4 

coo l e r t han no r m CI las t 0 f the Con tin n t l [) i v ; a. Coo lin w a 

raf.,lid in Dec~mber east of the Mi 1 "ippi. Th r w a com~l te 

a b sen ceo f t ro pic a l s tor m s in t h Gu t f f r. ' x 1 cor d C rib ban 

Sea dup to th unse so n bl intru ion 0 c ld ir aloft and the 

stronf)er than normal hi h- Ltiturl· 'J t rli 

J~Q~£C~ - The enti r e 

AtLantic (\.INA) wer 

MiddLe Atlantic 8inh t 

Gu lf of M 

son ll y 

nd h 

x;co 

col 

Gu I t 

t h t 

l a 

signific ntly colder th n r v r ge 

temperatures were found off hor 

3J/Ii to the Qffin of th ,uli of 

a l If fro 

loa large 

pat c h 0 f co L de r t h n ve r P. t m 

Scotia. The central Atlent;c ar 

be l 1,./ avera< e. 

The ,uLt Stream and slo~ ront 

conv luteo than they cd ee~ for th 

ctivity ~lso wa much r uc d. 

the Soutl, Atlantic 8; h he 

not resent 0 e 'Jee arlier. A f t 

3~ was the rem ins 0 warm cor, 

been extensively tudie cis ni 197 

391\!3C', D4 2L ' in July 1 7S end f 

moveo west ard u ti L December, an th n 

southwestward until it fi al y disBD r d 

eoge of tht:: shelf off t e DeL a va Pen;, uLa . 

s 

'.I S 

o r nin 

ov d 

t of 

ly bov 

f r 

t 

p r 

tou 

a rrr. eddy 

4QN, 66w was first bs rved ne r th nd 0 J nuary. Clo' co 

prevented its earLier lscovery, but stron OS 1 

~nomalies in th area in icat d t a i ao 

the montr. A cold eddy at 33 , 74 • s 0 ser ed 

last haLf of the month. 

lve 

o rm 

o r mHlg 

Storm centers crossed tt e U .<\. east CO s f a rther ort 

, n 

t 

usuaL, only one passino ~Out of Cepe 

SC). Another crossed the l wer Ches 

passed farther north. The Grand qan s 

ra s (n ar Charles on, 

Bay , nd t e 

r ecei ved a full measure 0 

severe storms this month. 

E~~[~2C~ - The Gulf Stream . a slightly of fs or of 

historical mean ~osition for the mont ost of the 

North Atlanti~ was warmer tha~ normal, u it a -5C anoma L 

cold patch at about 41~, 60W , and a cold remnant south of Cape 

Hatteras. The Gulf of Mexico was u to C lO\J nor al. The sea 

surface temperature (SST) was se sonal ly colder, in the ~ A, than 

'Last month by C.)C to as much a5 .7 C, while the Gulf was 

s L ; q h t L y 1,./ <: r me r t han Las t m 0 nth. 

Eddy activity more than doubled this month froffi last month, from 

one anticyc lonic and one cyclo ic eddy at t~e end of January t~ 

two anticyc Lonic and four cycLonic eddies in late February (\Jest 

44 
Paper 4 

of SSW). The Shelf Water/SlJpe water front also appeared more 

convoluted, although data were limited. A Shelf Water excursion 

pushed south~ast off the shelf abreast of Savannah, displacing 

the Gulf Stream. This excursion may have lasted up to two weeks, 

but cloud cover and differing interpretations do not allow 

complete definition. The SST anomaly off savannah was strongly 

negative, indicating that the feature was persistent. 

More storms than usual this month passed far north of normal and 

battered the North Atlantic shipping lanes. the u.s. coast south 

of Cape Cod was nearly storm free. One strong extratropical 

cyclone moved rapidly up the Piedmont early in the month, 

grounding an oil barge in Chesapeake Say on the 1st and a ship in 

Searsport, ME, on the 2nd. This storm raced northward and 

reached Davis Strait on the 4th. 

~gr£h - The western North Atlantic in £eneral was warmer than 

normal, with a small coLd anomaly patch remaining southeast of 

Nova Scotia. A tongue of cold water also wandered off the shelf 

east of Cape Charles, an expansion of the Savannah negative 

anomaly of Fenruary. Seasonal warminq was general throughout the 

GuLf of Mexico, though the anomalies remained negative except for 

small areas along the northern coast. Warming and cooling was 

uneven and indefinite in the wNA. 

Eddy activity continued to increa5e, showing one anticyclonic and 

five cyclonic eddies at the end of the month, plus the remains of 

the anticyclcnic eddy (ACE S) studie d by Bisagni (1976). The 

Gulf Stream moved slightly north during the month and became much 

more convoluted. 

Storms off the U.S. east coast formed farther east than 

and only one actually crossed the coast south of Long 

This ~as a minor storm over Cape Hatteras. The major 

grounds were nearly storm free. 

normal, 

Island. 

fishing 

~Qri! - The Middle Atlantic Bight area and eastward was up to 3C 

warmer than usual, with near normal temperatures to the south, 

and significant positive anomalies north of 3SN. A loop of warm 

Slope Water abutted the Gulf Stream at 37N, 72W, perhaps a 

consequence of reabsorption of an anticyclonic eddy. The pool of 

anomalously cold water southeast of Nova Scotia moved slightly 

eastward and deepened to greater than -4C anomaly. The sea surface in general was seasonally warmer than last month by O.SC to 

about 2C, though there was slight cooling in the area southwest 

of Bermuda. Lhe coastal positive anomalies in the Gulf of Mexico 

spread, while the central Gulf remained colder than normal. 

Although the number of Gulf Stream eddies decreased to only one 

small cycloni~ one at 34N30', 68W20' by the end of the month, the 

Shelf Water/Slope Water front was extremely convoluted and 

45 
Paper 4 

confused, as was the Gulf Stream front. Towards the end of the 

month warm tongues extended east of the Gulf Stream at 30N and 

33N, perhaps pr ec ursors to cyclonic eddy activity. 

The number o f storms was far below normal, rpsembling a summer 

month in the WNA. The storm tracks were concentrated north of 

Nova Scotia with only one crossing the coast to the south. A 

brief, severe extratropical storm caused the loss of the drilling 

rig Q~~!Q ~~~t~~s while under tow in the Gulf of Mexico. 

~gy - Although aLmost the entire WNA area unaer consideration was 

wa rmer this month, the change was seasonaL, and the warm SST 

ano malies decreased in extent and intensity. An area of negative 

anomalies east of the Gulf Str e am from 30N to 35N is a possible 

consequence of increased cycl onic eddy activity. The Gulf of 

Mexi c o was almost entirely colder than normal with positive 

anomalies o n Ly off FLorida ana in the loop current area. 

Th er e we re three small cyclonic eddies and one larger 

an t i cyclonic eddy, broken from a large Gulf Stream meander on 

10 May, present at th e end of the month. The Gulf Stream flowed 

smo o thLy to off Cape Charles, then began to meander downstream. 

How ever, t he meanders diminished in size as the month advanced. 

The Slope Water/Shelf Water front .as tortuous with incursions 

and e xcursions north cf 37N. 

Aga in this month there were fewer storms, and t~ese farther off 

the coast and farther north, than usual. One extratropical storm 

dev eloped in the central Gulf, crossed northern Florida, and then 

fo llowed the Gulf Stream across the Atlantic. 

~Q~ - The entire Atlantic area was 1 or 2 de£ warmer than last 

mo nth, as expected for the season. Positive SST anomalies 

diminished sLightly, and -3.3C anomalies appeared off the mouth 

of Chesapeake Bay. Neqative anomalies were found southeast of 

t he Bay to east of the Gulf Stream and southeast of Nova Scotia. 

The Gulf of Mexico was colder than normal over its entire area. 

Ed dy activity was apparently much reduced this month, though 

e x cessive cloudiness prevented clear sateLLite pictures of the 

Gu lf Stream ar.ea. The Coast Guard airborne radiation thermometer 

( ART) flights, also interrupted by bad weather, portrayed the 

west wall of the Gulf Stream generally following the 180 m 

isobath to Cape Hatteras, then bearing off northeastward to 37N 

and there turning to~ard the east to 71N, the limit of 

observations. There were also convoluted temperature patterns 

off Chesapeake Bay west of the Gulf Stream. Portions of the Gulf 

Stream, Slope Water, and Shelf Water regions were pictured by 

satellite late in the month. Strong meandering activity was 

found between 70W and 60W. One small cyclonic eddy was plotted 

in gyli~lr~Qm at 36N, 70W, its 29 May position, unsupported by 

46 
Paper 4 

SST anomaly or other evidence. 

Storm tracks were almost entirely north of 40N, with only one 

storm crossing the coast of Maine. The tracks curved northward 

between Greenland and the Faroes, and none crossed the British 

Isles or western Europe. 

~yly - The Gulf Stream this month closely followed the 18Q-m 

depth contour to Cape Hatteras, slightly inshore of its climatological mean position. Northeast of the Cape it followed the 

mean track to 70W, then meandered slightly downstream. The 

cyclonic eddy at 35N, 78w moved 2 deg westward during the month. 

There was much mixing of Slope and Shelf Waters during the month. 

Early in the month tremendous meanders and eddies developed, but 

all were apparently resorbed by the Gulf Stream. 

ALL SST's increased seasonally during the month, but the warm 

anomaLies diminisheo. A strong warm spot reached a +5C anomaly 

at 41N30', 64~30', with smaLler positive anomaly values north of 

39N from SSW to the American coastline. The rest of the Atlantic 

area was near normal for the month. The Gulf of Mexico remained 

anomaLously cold. 

Storm activity was beLow normaL this 

tracked west of the British IsLes. 

month, and most storms 

Over the Fourth of July weekend, mas se s of dead fish were 

reported oft Sandy Hook, NJ. Fisheries investigations 

(Armstrong, Paper 17) determined the cause to be an anoxic water 

mass, brought about by natural weather conditions, which expanded 

southward to AtLantic City, NJ, by mid-August, and by midSeptember covered ~alf of the Middle Atlantic Bight. Estimates 

were that up to 50% of the commercial fish stocks might be lost 

this year due to this phenomenon. 

~~g~~l - The Gulf Stream this 

imagery west of 60W. It 

historical mean track for the 

the south followed downstream 

month was fulLy seen by satellite 

flowed very smoothly along its 

month to 67W, then made a dip to 

by a larger one to the north. 

Two small cyclonic eddies persisted through the month, both 

moving about 150 km southwestward. A large (250 km diameter) 

anticyclonic eddy at 39N38', 67w originated on 25 August as a 

pinched off meander. A minor warm core eddy at about 38N30', 

72W30' shows on the ART isotherms as well as in the satellite 

analysis. The central ocean waters continued to warm at the 

surface this month, but SST·s over the continental shelf dropped 

due to tropjcal storm activity. In 1975, by contrast, seasonal 

warming persisted through Au'gust. Significant cold anomalies, on 

the order' of -1.5C, appeared in the Middle Atlantic Bight. 
Pa~er 4 

ExtratropicaL storms were concent rated from the Canadian 

Maritimes to the Denmark Strait, with a few storms crossing from 

ALaska to GreenLand. 

There were no ART flights east of Savann ah, GA, due to tropical 

stor ms. The u.s. east coast had no extratropical storms this 

month, but Hurricane Belle passed from Cape Hatteras to Long 

Island on the 9th and 10th. The Gulf of Mexico continued 

sLi g htly colder than normal. It spawned the weak tropical storm 

Dotti e , which crossed the southern tip of Florida and turned up 

the 80 th meridian to Charleston. 

~Q! mQ~r - Almost the entire North Atlantic surface area over 

the sheLf c~oled 1C to 2C this month. The warm anomaly area 

s out h of Nova Scotia expanded, but south of 40N, and in the Gulf 

of Me x ico, the SST's were average or slightly cooler than normal. 

The g~ lf~lr~am pictures a mildly meandering Gulf Stream for this 

month, wi th three cycLonic eddies and two anticyclonic eddies. 

SateL lite imagery intermittently pictured very complex eddy and 

meand ering activity. Cloud cover prevent ed proper definition, 

but th e patterns changed rapidly through the month, ending with 

the qu iete r conditions portrayed in g~lf~!r~£ m. In the middle of 

the mo nth t here were four anticyclonic eddies, one cyclonic eddy, 

and one cyclonic loop. There also were large patches of 

entrai ned SheLf Water and of mixed Shelf/Sl ope Water. One week 

Later onLy one anticyclonic eddy was found, along with two 

cyclon ic eddies and the one large cyclonic loop. There were 

still Lar ge patches of mixed Shelf/SLope Water, and the the Shelf 

Water/S l op e Water front was extremely convoluted. 

The onL y tropi cal st o rm in September remained completely east of 

61W. On Ly one st o rm was found reLativel y near the u.s. coast, 

and that one was stiLL offshore of the Gulf Stream. No n e crossed 

the coast SQuth of NewfoundLand, and most storms tra ck ed north 

between I ceLand and the Davis Strait. In 1975, by contrast, 

there were t hree major hurricanes; the extratropical storms 

tracked f a rther south and then between EngLand " and IceLand. 

There were no s torms in the GuLf of Mexic o in September 1976. 

Q£!QQ~r - The wa rm anomaLy area south of No va Scotia persisted , 

but th e re mainder of the AtLantic coastal area was not 

signif ic antLy warmer or colder than n~rmaL. The g~l!~!r~£m shows 

Large area s o f positive anomaLy, whi Le the temperature anomaLy 

charts s ho w Large areas of negative anomaL y. In the Gulf of 

~exi co , SST's were significantLy cooler than normal. 

The Gu lf Stream is pictured in g~lf~!r~2m fLowing smoothLy, with 

tw o ma j o r anticyclonic eddies. A coLd core eddy at 32N, 74w was 

en tire ly surrounded by warm Sargasso Sea Wa ter which reached to 

100 km f r om Cape Hatteras. The large warm eddy at 39N, 69W 
persisted, entraining SheLf Water 

smoothness of the Gulf Strea m 

definition caused by cLoud cover. 

on its 

front is 

eastern 

partLy 

edge. The 

due to poor 

Storm tracks moved farther south this month, anrl severaL storms 

passed up the u.s. east coast brin2ing winds above 70 kn 

(36 m/s), tornadoes, heavy rains, and flooding from South 

Carolina northward. The trawler k§Q§ £§rQl sank with a fuLL load 

of scaLlops off Barnegat Light on the 31st. Coast Guard 

heLicopters rescued the crew. The laden dragger E§lri£i§ ~§ri~' 

homeward bound to Provincetown ~ithin sight of other vessels, was 

lost with all hands (Schwadron 1977). 

A storm oevelcped on a cold front on the 16th, 350 km southwest 

of Ne~ Orleans, moved eas t-northeastNard across northern FLorida 

the next day, and raced along the classical storm track offshore 

to Nova Scotia and beyond on the 1bth. There was a second, 

milder storm in the western Gulf at the end of the month. The 

majority of the storms tracked significantly more easterly than 

in September, reaching the area between Greenland and Spain. 

~QY~mb~r - Due to surface mixing from intense cycLonic activity, 

the warm anomalies disappeared this month, and the sea surface 

was colder than normaL nearLy everywhere. Anomalies of about 

-3.5C occurred in the middle AtLantic Bight. T~e GuLf of Mexico 

continued about 1.5C colder than usual for the month. 

getween 5 0 and 60 km southeast of Cape Hatt eras, SST's rose 8C 

from west to east acro ss the west wall of the Gulf Stream. Both 

the ART and the g~li~tr~§m pictured an anticyclonic Gulf Stream 

loop in the South Atlanti c Bight. Due to cloud cover, eddy and 

meander observations were not clear. There was at least one 

anticyclonic eddy at 39N, 70~30·, and there may have been two 

more farther east. Last month's cyclonic eddy, with a noticeable 

warm ring, persisted at 35N, 71~. 

There was a succession of storms off the u.S. east coast this 

month. The first formed near Norfolk on the 5th, and in 24 hours 

was over Nova Scotia. The second formed off Cape Hatteras on the 

8th, paralleled the first slightly to the east, and reached 

Newfoundland the next day. Two more storms crossed New EngLand. 

At the end of the month a broad frontal area extended from the 

western GuLf of ~ex;co northeast to Nova Scotia. A succession of 

frontal waves and the long fetch of ~esterly winds created high 

seas and sweLls all along the front. The USCGC I§D~Y rescued the 

crew from a sinkin g shrimp boat 450 km northeast of NorfoLk. A 

storm which fermed in the GuLf of Mexico on the 13th under the 

influence of this storm system reached northern Greenland in six 

days. 
ExtratropicaL storms were concentrated from the Canadian 

Maritimes to thp Denmark Strait, with a few storms crossing from 

ALaska to GreenLand. 

There were no ART fLights east of Savannah, GA, due to tropicaL 

storms. The U.S. east coast had no extratropicaL storms this 

month, but Hurricane BeLle passed from Cape Hatteras to Long 

Island on the 9th and 10th. The GuLf of Mexico continued 

sLiqhtLy coLder than normaL. It spawned the weak tropicaL storm 

Dottie, which crossed the southern tip of Florida and turned up 

the 80th meri~ian to Charleston. 

~~Ql~mQ~r - Almost the entire North Atlantic surface area over 

the sheLf c~oled 1C to 2C this month. The warm anomaly area 

south of Nova Scotia expanded, but south of 40N, and in the GuLf 

of Me ico, the SST's were average or slightLy cooLer than normaL. 

The 9~!f~lr~am pictures a miLdLy meandering GuLf Stream for this 

month, with three cycLonic eddies and two anticycLonic eddies. 

SateLLite imagery intermittentLy pictured very compLex eddy and 

meandering cctivity. CLoud cover prevented proper definition, 

but the patterns changed rapidly through the month, ending with 

the quieter conditions portrayed in g~!f~lr~Qm. In the middle of 

the month there were four anticycLonic eddies, one cycLonic eddy, 

and one cyclonic Loop. There aLso were large patches of 

entrained SheLf Water and of mixed SheLf/Slope Water. One week 

Later onLy one anticycLonic eddy was found, aLong with two 

cycLonic eddies and the one Large cycLonic Loop. There were 

stilL large patches of mixed SheLf/SLope ater, and the the Shelf 

Water/Slope Water front was extremeLy convoluted. 

The onLy tropjcal storm in September remained compLeteLy east of 

61W. Only' one storm was found relatively near the u.S. coast, 

and that one was still offshore of the Gulf Stream. None crossed 

the coast SQuth of NewfoundLand, and most storms trarked north 

between IceLand and the Davis Strait. In 1975, by contrast, 

there were three major hurricanes; the extratropical storms 

tracked farther south and then between EngLand and IceLand. 

There were no storms ;n the Gulf of Mexico in September 1976. 

Q£!QQfr - The warm anomaLy area south of ~ova Scotia persisted , 

but the remainder of the Atlantic coastaL area was not 

significantly warmer or coLder than nJr~aL. The q~!f~lr~~m shows 

large areas of positive anomaLy, whi le the temperature anomaLy 

charts show large areas of neyative anomaLy. In the Gulf of 

Mexico, SST's were significantly cooler than normaL. 

The Gulf Stream ;s pictured in g~!f~!r~2m fLowing smoothLy, with 

two major anticyclonic eddies. A cold core eddy at 32N, 74W was 

entirely surrounded by warm Sargasso Sea Water which reached to 

100 km from Cape Hatteras. The large warm eddy at 39N, 69w 
persisted, entraining SheLf Water 

smoothness of the GuLf Stream 

definition caused by cLoud cover. 

on its 

front is 

eastern 

partLy 

edge. The 

due to poor 

Storm tracks moved farther south this month, and several storms 

passed up the U.S. east coast brin2ing winds above 70 kn 

(36 m/s), tornadoes, heavy rains, and flooding from South 

Carolina northward. The trawler ~2Q2 £2r21 sank with a fuLL load 

of scallops off Barnegat Light on the 31st. Coast Guard 

helicopters rescued the crew. The laden dragger E2!ri£i2 ~2ri~' 

homeward bound to Provincetown ~ithin sight of other vessels, was 

lost with all hands (Schwadron 1977). 

A storm aeveloped on a cold front on the 16th, 350 km southwest 

of New Orleans, moved east-nDrtheastNard across northern Florida 

the next day, and raced along the classical storm track offshore 

to Nova Scotia and beyond on the 10th. There was a second, 

milder storm in the western Gulf at the end of the month. The 

majority of the storms tracked significantly more easterly than 

in September, reaching the area between Greenland and Spain. 

~QY~IDb~r - Due to surface mixing from intense cycLonic activity, 

the warm anomalies disappeared this month, and the sea surface 

was colder than normal nearly everywhere. Anomalies of about 

-3.5C occurred in the middle AtLantic Bight. T~e Gulf of Mexico 

continued about 1.5C colder than usual for the month. 

getween 50 and 60 km southeast of Cape Ha tt eras, SST's rose 8C 

from west to east across the west wall of the Gulf Stream. Both 

the ART and the g~lf~tr~2m pictured an anticyclonic Gulf Stream 

loop in the South Atlantic Bight. Due to cloud cover, eddy and 

meander observations were not clear. There was at least one 

anticyclonic eddy at 39N, 70W30', and there may have been two 

more farther east. Last month1s cyclonic eddy, with a noticeable 

warm ring, persisted at 35N, 71~. 

There was a succession of storms off the u.s. east coast this 

month. The first formed near Norfolk on the 5th, and in 24 hours 

was over Nova Scotia. The second formed off Cape Hatteras on the 

8th, paralleLed the first slightly to the east, and reached 

Newfoundland the next day. T~o more storms crossed New England. 

At the end of the month a broad frontal area extended from the 

western Gulf of ~exico northeast to Nova Scotia. A succession of 

frontal waves and the long fetch of westerly winds created high 

seas and swelLs all along the front. The USCGC 12D~~ rescued the 

crew from a sinking shrimp boat 450 km northeast of Norfolk. A 

storm which formed in the Gulf of Mexico on the 13th under the 

influence of this storm system reached northern Greenland in six 

days. 

49 
rcqJCI .. 

Q~f~m~~~ - The SST's were not strikingly unusual this rrontr.. 

They tended to be slightly cooler than average north of Cepe 

Hatteras, with some warm anomaly water associated ith the 

warm-core eddies. The Gulf of Mexico continued cool. 

The GuLf Stream showed a meander east of Char lest n associated 

with the persistent cold eddy surrounded hy a ring of warm water 

at 33N, 7SW. A warm eddy also persisted at 39 , 72W. No others 

could be seen because of clouds. The Shelf I aterlSlope Water 

front in the Middle Atlantic gight was rag ed with incursions and 

excursions. 

A storm formed in South Carolina on the 7t , but was of li tle 

consequence in the western )rt Atlantic. Another formed off 

Georgia on t~e 15th, the day the ~r9Q ~~r~b~D! ran aground. I 

tracked rapidly northeastward, brin ing high winds and rough seas 

to the Nantucket Shoals area and reventing the Coast Guard from 

salvaging the oi l. 

Another storm, from the midwest, crossed he aine coast on the 

21st, affecting the same area Nith air tem ~ratures in the teens 

«-7C) and beLow, and causlng gales from Maine to Virginia. 

Another midwestern stor~ crosseo ew Jersey on the 28 hand 

turned northeastward, addina its fury to the shipping Lanes. The 

Panamanian tanker ~t~rrQ l~rritu was Last heard from 55 km fro 

Cape Sable. No trace of the ship has been found. 

LITERATJPE CITED 

BISAGNI, J. J~ 

1976. Passage of anticyclonic Gulf Stream eddies through 

deepwater aumpsite 106 during 1i74 and 1975. 'O AA Dumpsite 

Evaluation Rep. 76-1. 

SCHWADRON, S. 

1977. Loss of dragger 

Provincetown. Natl. 

and her cre~ i~ stunning 

Fisherman 57(9):25A, 31A. 

blow t::> 

3Sur veys in the area of the ~tgQ M~r~h~Q! spilL have shown 

mortalities and deformities among developing cod and pollock 

embryos, noticeable decreases in the abundance of sand lance 

larvae, and oil contamination of zooplankton. Studies are 

continuing; preliminary findings have been released in: The ARGO 

MERCHANT Oil Spill, NOAA Special Report, U.S. Dep. Commer., March 

1977. 

50 
Paper 5 

ANOMALIES OF MONTHLY MEAN SEA LEVEL ALONG THE 

WEST COASTS OF NORTH AND SOUTH AMERICA 

Date E. Bretschneider and Douglas R. ~cLainl 

INTRODUCTION 

Measurements of mean sea level provide a source of long-term 

information ~oncernin9 ocean processes. The data series of 

hourly tidal height measurements are unique among marine data 

series, in that they have been obtained inexpensively, over 

relatively Long periods, at many fixed locations worldwide. 

Many investigators have examined fluctuations of sea level at 

single stations, or reLationships among smalL groups of stations. 

Roden (196G, 1963, 1966) used spectraL and statistical methods to 

examine the interreLationships among sea LeveL, temperature, and 

atmospheric pressure at selected stations along the west coast of 

North America. Saur (1972) examined se a level differences 

between the Hawaiian IsLands and the Cal ifo rnia coast as an index 

of broad-scale changes in geostrophi c flow in the California 

Current system. For fisheries assessment purposes, however, 

monitoring of ocean changes requires groups of stations covering 

larger areas. The stations examined in this report extend along 

the west coasts of North and South America from Massacre Bay, 

Attu, in tne Aleutian Islands, to Caldera, Chile. 

DATA 

Most of the manthly mean sea level data in our data base were 

obtained from the University of Hawaii. 2 These data were updated 

I pacific EnvironmentaL Group, ~ational Marine Fisheries Service, 

NOAA, Monterey, CA 93940~ 

~e thank K. Wyrtki and B. Kilonsky, Department of Oceanography, 

University of Hawaii, who assembled these data and provided us 

with a tape capy. 

51 
and expanded with data from other sources. 

verted to centimeters. 

All data were conFor this report, tide stations most representative of open ocean 

conditions were s~lected. Although many tide gage stations 

examined in tnis report are l~cated on piers in sheltered coastal 

harbors, stations subject to highly variable local tidal 

conditions common to large river mouths (such as Astoria, OR), 

large shallow bays (such as Alameda, CAl, and straits or sounds 

(such as Ketchikan, AK), were generally not included. Additional 

criteria for station selection were a long, continuous data 

record, a constant tidal reference datum, and an even 

aistribution of stations with distance along the coast. The 

sta t ions selected and their locations are shown in Figure 5.1. 

The p rocesses affectinq sea level are complex. In addition to 

the well-understood tidal or astronomic forces, sea level is 

affected by: 

1. Changes in the average density of the water column. 

2. Changes in distribution of atmospheric pressure over the 

ocean surface (resulting, in part, in variations in large 

scale wiad patterns). 

3. Variations in s~eed of aLongshore components of ocean 

cur re n t s. 

4. Changes in total mass of ocean water 

accretion or melting of glaciers. 

resulting from 

5. Subsidence or emergence of the land upon ~hich the gage 

is located. 

The relative importance of these processes varies from station t o 

station. 

For ocpan monitoring in support of fisheries assessment, we are 

interested in fluctuations with periods of months to years. For 

this reason the data are presented in terms of monthly means 

which remove the principal diurnal and semidiurnal periodicities 

from the data. Fluctuations with periods longer than months or 

years can be reduced by c~mparing the data with a 19-yr mean. 

This compensates for the nodal tide, which results from the 

changing dectination of the moon over a period of 18.61 years. 

The nodal tide has a much greater "potential," or effect, than do 

3Permanent Service for Mean Sea Level, Berkenhead, U.K., and 

National Ocean Survey, NOAA, Washington, DC 20852. 

52 
other long-period, astronomicall y induced, harmonics observed in 

tidal data (Lisitzin 1974). we did not, however, remove very 

long-period fluctuations such as those caused by isostatic 

glacial responses (as at Yakutat, AK) or fluctuations related to 

land subsidence or uplift (such as at Balboa, CZ). 

Our objective is to compare temporal fluctuations of sea level 

along much of the eastern Pacific coast for eventual comparison 

with fishery fluctuati ons. In order to allo~ comparison between 

stations and to flag unusual events, the data are presented as 

monthly mean anomalies or departures of a given month from its 

long-term mean. The long-term means used in this report were for 

the 19-yr ~eriod, 1949-67. The tidal reference datum differs 

from station to station. Computation of anomalies at each 

station allows comparison in time between stations havinG 

different datum levels. 

Pattullo et ale (1955) found that in temperate and tropic 

latitudes (between about 40N and 40S) changes in the specific 

volume of the water column were responsible for most of tne 

nontidal variation in recordej sea level. Atmospheric pressure 

effects were found to account for only a small part of the 

recorded changes in sea level. This situation is not true, 

however, in higher latitudes. Lisitzin and Pattullo (1961) found 

that north of 4QN much of the variation in sea level results from 

changes in aistribution of atmospheric pressure over the ocean. 

This "inverted barometer" effect can be removed from the data in 

high latitudes by adjusting sea lev e ls for departures of 

atmospheric pressure from a long-term me an. 

There is evidence that fluctuations in atmospheric pressure are 

quickly followed by compensatin~ changes in sea level so that the 

total pressure on the sea floor remains very nearly constant. 

T~is isostatic adjustment is thought to occur over a range of 

severa l thousand miles and within a time span of several days. 

Thus, the ocean can be considered to approach isostatic 

equi l ibrium with atmospheric pressure for periods of a month or 

more . Assuming the average pressure over the oceans remains 

constant, if the pressure difference between two stations 

changes, the sea surface slope will change to compensate for this 

difference so that there will be no net change in the 

distribut ion of pressure on the sea floor (Pattullo et ale 1955; 

Saur 1972). 

Pressure effects were removed from the data by correcting sea 

levels to a long-term mean at~ospheric pressure in the vicinity 

of the tide gage. This compensates for both the normal seasonal 

cycle and the monthly pressure anomaly. Monthly mean sea Level 

pressure data were obtained ,from the World Weather Record series, 

53 
MonthLy CLimatic Data for the World, from CCEA, I or computed from 

monthLy mean pressure fields obtained from FN~C. 

Normal atmospheric pressures at each station were obtained by 

averaging monthly pressures for the entire period of record. The 

effects of monthly variations from this lona-term pressure mean 

were removed from sea level measurements by applying a correction 

of 1 cm in sea Level for each millibar deviation in dtmospheric 

pressure. Sea Level data for all stations north of azatLan were 

corrected in this manner, with rpsultant smaLL dec reases in the 

range of sea Level anomaLies. Pressure deviations south of 

MazatLan were on the order of one miLLibar or Less, not Large 

enough to warrant correction tecause sea LeveL measurements have 

a typicaL error of about 1 cm. 

DISCUSSION 

The a nomaLies of corrected monthLy mean sea LeveL (Figs. 5.2-5.6) 

exhibit remarkabLy coherent patterns in time and space. Perhaps 

the most striking feature of the time series is the Long-term 

persistence and wide distribution of high sea LeveL during the 

period 1957-59. Evidence of anomaLousLy high sea LeveL extenos 

from Caldera, ChiLe, to Adak, AK. Similar periods of anomalously 

high sea LeveL can be seen in 1940-41 and 1971-73, and to a 

lesser extent in 1951-52 and 1965-66. 

The simuLtaneous occurrence of these changes over such vast 

distances suggests a reLation to Large-scaLe oceanic or atmospheric disturbances. The periods of anomaLousLy high sea LeveLs 

were aLso periods of anomalousLy warm sea surface temperatures 

and are associated with El Nino occurrences in the eastern 

tropicaL Pacific (Quinn 1976, 1978). 

Such environmentaL changes can have dramatic effects on marine 

fis~eries. ALong the coast of Peru, for exampLe, Large changes 

in the distrlbution and abundance of anchoveta resuLt from 

adverse oceanographic conditions associateo with EL Nino periods. 

These conditions, combined with heavy expLoitation, have resuLteo 

in a decline of the fishery and have had major economic impact. 

Radovich (1961) documented many changes in the distribution of 

marine populations along the coast of CaLifornia durina the warm 

water periods 1940-41 and 1957-59 which were associated~with high 

sea leveLs. He found a general northerly shift of southern 

·Center for Climatic and Environmental Assessment, Environmental 

Data Service, NOAA, Columbia, MO 65201. 

5Fleet Numerical Weather Central, U.s. Navy, Monterey, CA 93940 . 

54 
species and an increase in yell~wtail and bonito populations off 

California. Changes of sea level related to fluctuating coastal 

circulation may be associated with variations in year class 

strengths of marine populations due to changes in larval 

transport. 

In his investigation of lo~ frequency sea level oscillations, 

Roden (1966) found a high coherence in sea level fluctuations 

measured by tide gages located within similar macroenvironments, 

such as tho~e located within the Gulf of Alaska or within the 

California Current area. Even stations with dissimilar exposure, 

such as tho~e with gages located on the open coast compared to 

those with gages located in enclosed bays, yielded similar 

results if the stations were within the same macroenvironment. 

We now examine fluctuations of sea level in groups of stations 

having similar oceanographic environments. 

Sea levels in this area are quite variable. Significant longterm lower sea levels can be seen at Adak (1943-51) and Attu 

(1952-53). In contrast to the low sea levels observed at Adak 

and Attu in 1952-53, Unalaska, Kodiak, and Yakutat show 

ano~alously high values, with a peak in early 1953. There seems 

to be little correlation between Attu and neighboring stations. 

This suggests that sea level at Attu, which is located in an area 

of relatively free exchange between the Pacific Ocean and Bering 

Sea, may respond to a different comb in ation of environmental 

processes than sea level at Adak, Una laska, or Kodiak. It is 

interesting to note that Attu is the only station of the 25 

examined that did not show anomalousLy high sea levels in 

1 957-5 9. Unalaska had small anomalies through 1956 and strong 

positive anomalies during 1957-59. In contrast, the periods 

1964-67 and 1971-74 exhibit strong negative anomalies. This 

suggests long-term fluctuations in the ocean environment near 

Unalaska. 

Kodiak has the shortest record of observations in the series. It 

was included to fill a gap between widespread stations. It shows 

surprisingly small variations in sea level with extremes in 

1957-58 and 1961-62. A weak positive anomaly with a peak in 

early 1958 is evident. 

The Yakutat gage, located in a harbor, is subject to salinity 

changes due to increased river runoff during summer months 

<Favorite 1974). The trend of decreasing sea level seen in the 

series for this station results from land uplift due to isostatic LaciaL rebound. Strong negative anomalies are evident during 

1955-56, 1961-62, and 1971-72. Surprising small positive 

55 
anomalies are seen during 195B. Fdvorite (1974) has shown that 

annual mean sea level anomaLies at Yakutat were well correlated 

with mean annual wind stress transport anomalies in the Gulf of 

Alaska during the period 1950-59. 

Fairly persistent long-term sea level anoma lies with short-ter 

fluctuations can be seen at Sitka, Prince Rupe rt, Tofino, Nea 

Bay, and Crescent City. Sea level fluctuationS are remarkably 

coherent amoog these stations, considering the 1800 km along the 

coast between Sitka and Crescent City. Majo r periods of high sea 

Level are seen during 194C-41 and 1957-50. Low sea leveL periods 

incLude 1955-56, late 1~61-early 1962, and 1964. A significant 

p riod of anomalously low sea level is evident at Prince Rupert 

~etween the years 1947 and 1951. 

Sea level data from San Francisco, Avila Beach , Los Angeles, and 

La Jolla elso exhibit simiLar fluctuations. Pe riods of high sea 

leve l are noticeable during 1941, 1951-52, 1957-59, and 1972-73 

a t all stations. Periods of hi h sea level during 1969 were 

observed at San Francisco and Avi lao Periods of low sea level 

o cc rred at all stations during 1955 and early 1956 and during 

1964. A strong trend of rising sea level in relation to land 

occurred at all stations in this group. 

Mazatalan, ~anzanillo, Aca~uLco, EaLboa , La Un ion, and 

Buenaventura show simiLar ~atterns of sea level fLuctuations. 

Periods of high sea leveL correspond very weLL with El in o 

conditions (~uinn 1S76, 1978). ALL stations exhibit very high 

sea levels during 1941-42, 1957-59, and, ~o a Lesser extent, 

1965-66. Extremely high levels ~ere noted during 1972-73. The 

anomaly at Manzanillo for December 1972 measured 2&.8 cm, one o f 

the Largest in the entire series. Anomalous ly low sea level s 

were seen i~ 1949-5C, 1955, and 1967. The station at Balboa 

shows a treod of rising sea level which Roden (1963) attributed 

to land subsiaence. 

Talara, Callao, Matarani, Antofagasta, and Caldera also show 

remarkably coherent fluctuations in sea level. Like the group of 

stations to the north, ppriods of high sea level correspond weLL 

with EL Nino conditions. The 1941-42 per iod of high sea leveLs 

is evident at Matarani. The 1957-59 and 1965 periods of hi~h sea 

LeveLs are £een at aLL stations in this regi~n. During 1972, a 

period of extremeLy high sea levels occurred at Talara peaking at 

36.5 cm in December 1972. A maximum anomaly of 34.4 cm was 

measured at Talara during November 1974. It is interesting to 

56 
note the sharp spike of extremely low sea level that occurred 

just before the 1974 period of high sea level at TaLara. 

Anomalously bigh sea levels are also evident at Callao during 

1972. Periods of low sea level occurred at all stations in this 

group during 1949-50, 1954-56, and 1966-67. 

CONCLUSION 

Anomalies of monthly mean sea level observations along the west 

coast of ~ortb and South America persist for periods ranging from 

several month£ to two years or longer and are coherent in s~ace 

for hundreds of kilometers. Anomalous "events" can be traced 

along th~ coast from Chile to Alaska and may be related to 

coastal circulation processes which may in turn affect larval 

drift and reproductive success of marine organisms. Certainly 

the major periods of anomalously high sea level during 1941-42, 

1957-59, and 1972 were associated with unusual changes in the 

abundance or distribution of many marine species. It is hopec 

that further research on the factors affectin g sea leveL will 

lead to ~ better understanding of ocean circulation processes and 

their effects on populations of marine organisms. 

LITERATURE CITED 

FAVORITE, F. 

1974. On flow into the Bering Sea through Aleutian Islana 

passes. In D. W. Hood and E. J. Kelly (editors), Oceanography of the Bering Sea. Occas. Publ. No.2, Inst. Mar. 

Sci., U. Alaska, Fairbanks. 

LISITZIN, E. 

1974. SeaLevel 

286 p. 

changes. Elsevier 

LISITZI N, E., and J. G. PATTULLO. 

sci. Pubt. Co., N. Y • , 

1961. The principal factors influencing the seasonaL 

oscillation of sea level. J. Geophys. Res. 66:845-852. 

PATTULLO, J., W. MUNK, R. REVELLE, and E. STRONG. 

1955. The seasonal oscillation in sea leveL. 

14:88-155. 

57 

J. Mar. Res. 
Paper 5 

QUINN, W. H. 

1976. El Nino, anomalous Equatorial Pacific conditions and 

their prediction. In J. R. Goulet, Jr. (compiler), The 

environment of the United States livin£ marine resources1974., p. 11-1--11-18. U.S. Dep. Commer., Natl. Oceanic 

Atmos. Admin., Natl. Mar. Fish, Serv., MARMAP (Mar. Resour. 

Monit. Assess. predict. Program) Contrib. 104. 

1978. Equatorial Pacific anomalies and EL Nino. In J. R. 

Goulet, Jr. and E. D. Haynes (editors), Ocean variability: 

Effects on U.S. marine fishery resources - 1975, p. 179-

190. U.~. Dep. Commer, ~OAA Tech. Rep. NMFS Circ. 416. 

RADOVICH, J. 

1961. Relationships of some ~arine organisms of the northeast 

Pacific to water temperatures, particularly during 1957 

through 1959. Calif. Dep. Fish Game, CaLif. Fish Bull. 

112,62 p. 

RODEN, G. I. 

1960. On the nonseasonal variations in sea leveL aLong the 

west coast of North America. J. Geophys. Res. 65:2809-2826. 

1963. Sea level variations at Panama. J. Geophys. Res. 68: 

5701-5710. 

1966. Low-frequency sea Level osciLlations along the Pacific 

coast of North America. J. Geophys. Res. 71:4755-4776. 

SAUR, J. F. T. 

1 97 2 • Mont h l y sea 

Islands and the 

619-{)36. 

level differences 

California C9ast. 

58 

between the Hawaiian 

Fish. Bull. u.s. 70: 
o 

Kodiak, 

Attu, AK .0 

o .·.·Unalaska, AK " ' 0' 

Adak, AK 

AK 

AK 

Rupert, B.C. 

Cit Y , 

Los Angeles, 

San Franci sco, CA 

Avi la, CA 

La Jolla, CA 

Mazat lan, 

Man z a n-i 1 1 0, Me x . 

Acapulco, Mex. 

La Union, EI Salv. 

Talara, 

Ca Ilao, Peru 

Ant of agasta, 

Caldera, 

Figure S.l.-Selected tide stations along the west coast of North and South America. 

59 
§ 

RTTU. RLRSKR 52- 50N 173-12E 

2e 

10 

o I I I I I I I I I I I I I I I I' ,1 "I If 411141f ' 'I . 11111 \ I. 'lilI""'il" li' III 

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- Ill 

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m 

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: fl 36 37 3B [rrj42[L ,]IDI1I ]~IIJJIUDIjlwQ['1~~76 

I , 

TOFINO.CRNROR 49- 09N 125-55W 

" III I II 1.1111411.11 .I. I II Ill! 111111'1111. 

I - Ill T 

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Figure 5.3.-Anomalies of mean sea level for stations in the Gulf of Alaska and Pacific Northwest. 
0) 

t.:> 

SAN FRANCISCO. CALIF 37-48N 122- 28W 

2lII 

L" 

" 

-111 

AVILR 35-10N 120-44W 

2lII -9132.33 3.i 3536373839 .i"-l .i1 

I" 

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RCRPULCO,MEX 

2Il 

III 

II I I III ++-+-+--+ I I III -ht 

Figure 5.5.-Anomalies of mean sea level for stations in Mexico and Central America. 

76 

76 

I I 
:t.: 

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1111 

III I I I 1

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::: ~ I I I I I I I I I I I I I I I I I I' I I i I I I!, 
Pap e r 6 

COASTAL UPWELLING OFF WESTERN NORTH AMERICA, 1976 

Craig s. Nelson i 

INTRODUCTION 

The nearshore marine environment off western North America is 

markedly influenced by processes of coastal upwelling and 

downwellin9. Upwelling is widely recognized as a fundamental 

factor in the formation of nutrient rich surface water favorable 

to primary production. Wind induced surface layer divergence may 

also dramatically modify nearshore marine climate, and may act as 

an important driving mechanism for continental' shelf/slope 

ci rculation. 2 

Variations in biolog ical communities often occur nearly in phase 

with the predominant seasonal cycle of coastal upwelling. Major 

fLuctuations in the intensity of coastal upwelling also occur at 

frequencies corresponding to the diurnal sea breeze, to synoptic 

"events", and to interyear variations i n the location and 

intensity of the large scale atmospheric c ir culation system over 

the northeastern Pacific. Anomalously stron g or weak upwelling 

may be relaLed to major fluctuations in stock recruitment 

(Parrish 1976) which are likely to have subsequent effects higher 

in the food ch a in. 

Bakun (1973) com puted an index of coastal upwelLing based on 

calculations of surface wind stress derivea from analyzed fields 

of surface atmospheric pressure. These fields a,re routinely 

oroduced by the U.s. Navy Fleet Numerical Weather Central. The 

"uPwelling index" is defined as the offshore directed component 

of Ekman transport, and is considered to be a gross measure of 

the amount of upwelLing required to replace water transported 

offshore in the surface layer. Negative values of this index 

iPacific Environmental Group, National Marine Fisheries Service, 

NOAA, Monterey, CA 93940. 2 N;iler, P. P., and C. N. K. Mooers. 1977. A model shelf 

dynamics pro~ram. A report to the NationaL Science Foundation, 

Office of the International Decade of Ocean Exploration, January 

1977. 

65 
indicate onshore surface transport and do~nweLLing at the coast

Monthly mean upweLLing index vaLues for the period 1946-71 were 

presented for the 15 Locations shown in Figure 6.1. These timE 

series have been updated for 1972-74 and 1975 (Bakun 1976, 1978) 

MonthLy upweLling indices for 1976 are given in TabLe 6.1 

AnomaLies from the 20-yr (1946-67) mean monthLy vaLues ar 

presented in TabLe 0.2. UpweLLing indices are dispLayed i 

percenti Les in Figure 6.2. Percenti Le vaLues were based on th 

rank of the upweLLing index for each month and Location withi 

the 31-yr (1946-76) time series. 

THE GULF OF ALASKA 

~ind driven surface transport in the GuLf of ALaska (60N, 149W t 

51N, 171w) tends to be divergent in the interior and convergen 

at the coast. 3 The annuaL cycLe of coastaL convergence i 

dominated by vigorous downweLLing during the winter season, whe 

intense cycLonic storm activity characterizes the atmospheri 

circuLation in the region. During 1976 monthLy upweLLing indice 

were negative aLong both northern and eastern boundaries, excep 

in June and JuLy when smaLL positive vaLues were evident. 

In January more intense than normaL downweLLing was indicate 

aLong the ea~tern boundary, NhiLe positive anomaLies occurred i 

the northern Gulf of ALaska. This pattern of anomaLies reverse 

the trends for these two areas begun during the Last quarter 0 

1975 (Bakun 1978). The remainder of the first quarter of 197 

was marked by Less intense than normaL winter downweLLing 

Reduced LeveL& of coastal convergence may be associated with Les 

intense than normaL surface divergence offshore. A decrease i 

the strength of the coupLed "pu'llping" between the centraL GuLf 0 

ALaska and the coast wouLd tend to reduce the barocLinicit 

estabLished during the previous three months. 

More intense than normaL coastaL convergence was evident durin 

the remaining months of 1976. A generaL pattern of upweLLin 

indices beLow the median (Fig. 6.2) was interrupted in June, whe 

smaLL positive vaLues occurred, and in October, when an irreguLa 

transition to vigorous winter downweLLing was apparent 

AnomaLies from the Long-term monthLy means (TabLe 6.2) we~ 

negative from ApriL through September, except during June, a 

3 Ingraham, W. J., Jr., A. Bakun, and F. Favorit e. 1976. 

Physical Oceanography of the GuLf of ALaska. U.S. Dep. Commer. 

NOAA, N~iFS, Northwest Fish. Cen., Processed Rep., 132 p. 

66 
paper 6 

these five locations. Upwellin~ indices at 54N, 134W and 51N, 

131W for May and July were the lowest (largest negative values) 

calculated in the 31-yr time series. Coastal convergence 

continued th~ough the summer at approximately one-half the 

intensity of the preceding winter's downwelling. Under these 

conditions, the existing baroclinic structure would tend to be 

maintained. Ihis situation contrasts with more typical relaxed 

summer conditions, in which the baroclinicity established during 

a previous winter is dissipated. 

A smooth transition to vigorous winter downwelling was replaced 

by less intense than normal d~wnwelling in October. This period 

of positive anomalies immediately followed and preceded several 

months of large negative anomalies. An examination of the 

monthly mean surface atmos~heric ~ressure field for October (not 

shown) indicated a westward shift, relotive to the long-term mean 

position, of the center of the low pressure system and a much 

reduced pres~ure gradient near the coast. A return to near 

normal (50th percentile) winter down~elling occurred in December. 

VANCOUVER ISLAND TO POINT CONCEPTION 

The stretch of coast from Vancouver Island (48N) to Point 

Conception (16N) is a transition zone, in which wind driven 

surface transport changes from predominant ly onshore to 

predominantly offshore. During 1976 thi s entire coastal region 

was characterized by a pattern of thr e e periods of more positive 

than normal upwelling indices separated by two short intervals of 

more negative than normal indices. These features repeat the 

general pattern noted in the previous section, and indicate a 

deQree of coherence in the large scale atmospheric circulation on 

space scales approaching 1,200 km and on time scales of two to 

four months. 

~~gh ~g~ tQ £~Qt[~l Q[~~QQ i~~~~ lf~~ lQ ~~~~ lf~~l. Large positive anomalies in January extended a period of relaxed 

coastal convergence first noted in December 1975 (Bakun 1978). 

This trend did not continue; near normal downwelling was 

indicated fram February through April along the coasts of 

Washington and northern Oregon. A prolonged period of relaxed 

coastal upwelling from May to September was interrupted in June 

by a return to near normal index values. However, this feature 

appeared as an anomaly in a pattern of upwelling indices below 

the median, in a region stretching from the northern Gulf of 

Alaska to Oregon. Upwelling peaked in June, somewhat earlier 

than the long-term mean values would indicate (Bakun 1973). FalL 

and early winter were characterized by a return to negative mean 

values (coastal convergence), although positive anomalies 

indicated less intense than normaL downwelLing. 

____________________________________ 2_ ______ ~ ________________________________ _
Paper 6 

~gg~ §l~u~Q ~ EQiu! £Qu£~~!iQU 1~~~~ 1,2~!Q ~Q~~ 1~'~1· The 

patterns of positive anomaLies during winter and negative 

anomalies during summer noted above were not repeated exactly 

along the coasts of southern Oregon and northern CaLifornia. 

This stretch of coast encompasses the cor~ of the CaLifornia 

Current upwelling region, which is characterized , in the mean, by 

a maximum in the alongshore com~onent of surface wind stress 

during JuLy (Nelson in press). In 1976 the timing, duration, and 

intensity of the indicated upwelLing at Cape BLanco (42N), Cape 

Mendocino C39N), and to a lesser extent Point Conception (36~), 

were markedly different than the 1946-67 long-term mean 

conditions. 

Pos i tive anomalies occurred in January and February, during a 

part of the year ordinariLy characterized by coastaL convergence. 

ALtho u gh onshore transport was indicated at 42t, upwelling 

indices for 39N were positive and were clearly atove the 5~th 

percentiLe. This feature continued a long trend of positive 

anomaLies which began in A~riL 1975 <oakun 1970). 

The onset of anomaLous upweLling a~peared to occur rather 

abruptLy in March. The timin g of this event was coherent at 

thr e e Locations aLong the coast (Fig. 6.2). ear Cape endocino 

( 39N), the March index was nearly a factor of three greater than 

the long-term mean value for this month and location. A retur 

to near normal conditions occurred in April. 

Conditions favorable to strong coastaL upwelling reappeared in 

May, June, and July. Monthly mean indices exceeded the Seth 

percentiLe at both 42N and 39N. The vaLues computed for Cape 

Mendocino (39N) were the second highest in ~ay, and the thirc 

largest in June within the 31-yr series. This recurrence of 

unusuaLly Large positive anomalies markea the fourth consecutivE 

year in which stronger than normal coastal divergence has beer 

indicated. Such Long-term persistence possibly suggests either a 

shift in, or intensification of, the Large-scale atmospheric 

circulation influencing the west coast of North America. The 

timing of the summer upwelLing season was also somewhat unusual. 

Index values peaked in May, two months earLier than the peaks in 

the long-term mean cycLes for these Locations. 

A rapid transition to beLow normal upweLling (i.e., negative 

anomalies) during August was i~mediateLy foLlowed by a return to 

large positive anomaLies in September. The period of reLaxed 

upwelling in August was notable, since negative anomalies during 

this month were evident along the entire stretch of coast from 

the northern Gulf of Alaska to the Southern California Sight. 

The pattern of positive anomaLies persisted through the last 

quarter of 1976. While the upweLling indices at 42N approached 

the 20-yr mean values (i.e., downwelLing), indices exceeding the 
r 0 I

 ~ ~ U 

80th percentjle occurred in September and October at Cape 

Mendocino. The indices for November and December showed a 

gradual return to median values; however, upwelling was still 

indicated for 39N. As Bakun (1978) has already noted, such a 

prolonged period of upwelling would appear to be favorable for 

hose fish stocks dependent upon upwelling based primary 

roduction. 

POINT CONCEPTION TO BAJA CALIFORNIA 

secondary California Current upwelling regime along this coast 

(33N, 119W to 21N, 107W) is characterized by positive values of 

offshore transport throughout the year (Bakun and Nelson in 

press). Maximum upwelling index values occur from March to May 

and coincide, in time, with major peaks in spawnin~. 

Although the ~pwelling index remained positive during 1976, the 

most prominent features were the extended periods of large 

negative anomalies in January and February, and again from August 

to December. This pattern marked an almost complete reversal of 

the conditions which prevaiLed in 1975. During the previous 

y ear, below median values occurred in summer, while above median 

indices were evident in spring and fall. 

Positive monthly mean anomalies were evident from March to August 

(Table 6.2). Much more intense than normaL upwelling at 

l ocations from Punta Eugenia (27N) to Cabo San Lucas (21N) 

xtended the upwelling season to late summer. This period was 

i mmediately followed by a decline to large negative anomalies. 

r his pattern of negative anomalies during fall and early winter 

encompassed the entire region from Point Conception (36N) to Cabo 

San Lazaro (24N). Upwelling indices were consistently below the 

30 th percentile, which suggested extremely r e laxed upwelling for 

th is time of year. 

The pattern of negative anomalies corresponded in time and in 

l ocation with a rapid warming of surface water during fall and 

winter. The intensity of warming was indicated by December sea 

s urface temperature anomalies 2C warmer than the 1946-67 mean, 

and more than 3C warmer than the temperatures during the 1975 

winter season.4 Relaxed upwelling (i.e., small values of 

o ffshore transport) is correl3ted with northward surface flow 

4fi~hjQg InfQrm21iQO' No. 12, December 1976. Southeast 

F ish e r i esC e nt e r, N M F S, N 0 A A,. L a J 0 II a, C A 9 2 03 8 • 

69 
near the coast. The upw llin 

1976 indicateu the possibi Lity 

southern water which could hav 

condit lor 

of 

)( t n 

durin fall and wint!r 

jo r intru ion of w r 

b yone oint Cone ptlon. 

RELATI TO FISH IES 

',J i t h i nth e c oa s taL ri o n fro Po; teo n c 

Lucas (21~), upwellin nd ~pw lling r 

important transport mech n; ms for fi h 

area. The five m nt S o f Lo nor 

foLLoloied a eriod of moderate l lLi 

bas is of b ve normaL up Ll"ro 

spawn;n, recruitment m d ls r 

re roductive success for ~acific 

upwellin during th fall nd 

coast would tend to f v r 

S t 0 C k 0 f P ac i f i c mac r L, 

inc r e (l set h est i In a t s f 

predicted on the basis of spr;n 

evidence ind; cat s that, lnd 

stronQer t an had e n antic; t 

SNelson, C • .). 1976. Seasonal variations 1n rocesses reLate 

to the CaLifornia Current. Paper presented at the 23 r a Easte r fl 

Pacltic Oceanograph ic Conference, Septem e r 29 - cto e r 1, 1976 . 

6Parrish, R_ H., and C. S . Nelson. Fish s tocks and th e 

CaLifornia Current. Faper presented at the CaLif . Coop . Ocea nic 

Fish. Invest. Conference , ovember 16-18, 19 76 , Palm Sp rin gs , CA. 

U npub l. manu scr. 

7R. H. Parrish, Pacific Envi r onmenta l Group , MFS , NOAA, 

Monterey, CA 93940. Pers . com~un. 

SR . A. Klingbei l, Cc litornia Fish and Game Comm ., Long Be ach, CA 

90802. Pers . COMmun. 

70 
0 J t, U 

LITERATU~E CITED 

BAKUN, A. 

1973. Coa~tal upwelling indices, west coast of North America, 

1946-71. u.s. Dep. Commer., NOAA Tech. Rep. NMFS SSRf-671, 

103 p. 

1976. Coast.aL upweLling off western North America, 1974. 10 

J. R. GouLet, Jr. (compiLer), The environment of the United 

states living marine resources - 1974, p. 12-1--12-16. U.S. 

Dep. Commer., Natl. oceanic Atmos. Admin., NatL. Mar. Fish. 

Serv., MARMAP (Mar. Resour. Monit. Asses. Predict. Program) 

Con t rib. 104. 

1978. Coa~tal upweLLing off western North America, 1975. 1u 

J. R. Goulet, Jr. and E. D. Haynes (editors), Ocean 

variability: Effects on u.s. marine fishery resources1975, p. 141-149. u.s. Dep. Commer., NOAA Tech Rep. NMFS 

Circ.416. 

AKUN, A., and C. S. NELSON. 

In press. CLimatoLogy of upwelLing related processes off Baja 

CaLifornia. Calif. Coop. Oceanic Fis~. Invest. (CalCOFI) 

Rep. 

NELSON, C. S. 

In press. Wind stress and wind stress curl over the California 

Current. u.s. Dep. Commer., ~OAA Tech. Rep. NMFS SSRF. 

PARRISH, R. H. 

1976. An 3ssessment of environmentall y related variation in 

the recruitment of the California Stock of Pacific mackerel 

(~£QmQ~r iaQQoi~~~) and its implications for management. 

Ph.D. Thesis, Oregon State University, Corvallis, 111 p. 

71 
Table 6.1 - M0nthly coastal upwelling indices for 1976. Units are cubic meters 

per second per 100m length of coast. Negative values indicate onshore transport 

of surface waters and resultant downwelling. 

JAN FEB MAR APR l:ffiY. JUN JUL ...ru&. .sEe. .Qtl .JiQ.V.. ..12K 

60N 149W -85 -91 -10 -16 -2 4 2 -1 -17 -12 -68 -94 

60N 146W -113 -104 -13 -26 -4 8 2 -2 -33 -22 -123 

57N 137~~ -201 -50 -35 -54 -':til 6 -6 -8 -81 -58 -237 -1 

54N 134W -159 -18 -40 -"" -'l'l 5 -26 -7 -56 -39 

"51N 13HI -81 1 -16 -33 -21 20 -23 4 -12 -6 

48N 125~J -63 -35 

45N 125H -41 

42N 12514 -10 -4 
Table 6.2 - Monthly coastal upwelling index anomalies for 1976 relative to the 

20-year (1948-67) mean value for each month and location. Units are cubi c 

meters per second per 100 m length of coast. 

JAN FEB MAR APR MAY JUN JUL AUG SEP OCT NOV DEC 

60N 149W 54 -5 36 -5 -2 -2 -4 -6 -14 14 5 14 

60N 146W 67 -2 35 -14 -2 -3 -5 -24 12 -29 -17 

57N 137W 11 67 16 -30 -25 6 -8 -2 -52 29 -96 31 

54N 134W - 63 49 -12 -35 -46 5 -29 -7 -33 43 -65 5 

51 N 131 W - 17 37 -4 -27 -25 5 -39 -9 -9 34 -10 9 

48N 125W 27 12 -3 -3 -11 5 -29 -13 -3 33 51 47 -J 

c.:> 

45N 125W 53 18 5 -9 -13 8 -51 -34 -3 20 42 46 

42N 125W 57 24 16 -18 53 63 -36 -47 16 7 19 31 

39N 125W 21 0 65 -10 207 136 68 -28 71 59 8 16 

36N 122W 12 -15 44 -5 56 -43 25 -73 -14 0 -8 -6 

33N 119W -20 -14 -0 20 21 -50 46 -0 -49 -26 -1 8 -16 

30N 119W -12 -14 23 19 31 -0 17 3 -59 -23 -11 -26 

27N 116W - 45 -43 8 10 13 19 28 65 -54 -48 -46 -46 

24N 113W -26 -24 34 36 49 44 59 42 8 3 -19 -8 

21N 107W 3 -7 25 25 32 -3 27 -2 1 5 31 10 26 
} :fIi: I:::::::"::::':':: :::;:': ":';;:::.::; :,. ';:;:. ; .' .' ::' .; I t I:: l 

!!!!I;~lll: H "'I'ea 149 14E 143 I .. k> t. ~r "14 ~J ~8 I ~5 f2.2 119 1I6i 113 tl b ~ ~~1)f 

6~ I:::: I·:: : .:. 

)i: I::::' ~ ~ 

::: _.JrY ~~. iLO:~ k, 

j~ ~ ,. "pr 1 

~tJ I 

!\'-

~ ~ t\ 1 

'~' 

~. : : 

, 

54 \ 

I'~~ ! 

z '\ 

51 I 

L ' , 

- t- + 

f~ i- f-t- I- e48 I ~ ":' 

-: 1 

45 I I 

42 I 

I 

- -- - - ! 39 I ~f: 

36 --" - ~ 

33 

.,,... , t ..JV 

. ~ 

, , " J ~. 

27 . I ~' ---'---_ . !-- r f- .;-:-'- 24 '" ! 

'" "" -:~ 21 

f- r-+- - t- ~ D " 18 ~ 

t I + l- t- t -

I 1 I 

Figure 6.1.-Computation grid. Intersections at which upwelling indi ces ar e computed are marked with large dots. 

74 
~ERCENTILIZED MONTHLY MERN UPWELLING INDICES 

0N,149W 

,0N,146W 

7N,137W 

4N' 134W 

ilN,131W 

8N, 125W 

f5N,125W 

l2N,125W 

N,125W 

6N,122W 

3N,119W 

~N,119W 

7N,116W 

4N,113W 

1 N, 107101 

1976 

J F M R M J J R 5 

95 

igure 6.2.-Percentalized upwelling index values for 1976. Percentil es indicate relathe ranking Wlthin the 31-)T data (or each month 

and location. The contour interval is 10 percentile unit s. Yalue below the median (50th perc ntlJe are aded 

75 

Paper 7 

OCEANIC CONDITIONS DURING 1976 BETWEEN 

SAN FRANCISCO AND HONOLULU 

AS OBSERVED FROM SHIPS OF OPPORTUNITY 

J. F. T. Saur 1 and D. R. McLain 2 

INTRODUCTION 

Durin~ 1976 cooperating merchant ships continued to make sections 

of surface &alinity samples and of expendable bathythermograph 

(XBT) observations on the San Francisco-Honolulu ship route 

(Fig. 7.1). Similar sections of observations were obtained most 

of the year, but less frequently, on the seattle and Los Angeles 

t o Hawaii rcutes. These, however, were discontinued at the end 

of October far lack of funds, and these two routes are not 

c onsidered in this paper. The sompling was done for the National 

Marine Fisheries Service using funds provided by the National 

Science Foundation under the NORPAX program. 

The San Francisco-Honolulu route cross e s a Transition Zone whic h 

Lies between the cooLer, lower sa l ini ty , modified subarctic 

1)01 ate r s 0 f the Cal i for n i a Cur r e n tan d the war mer, h i 9 her sal i nit y 

IrJ ate r S 0 f the E a s t ern Nor t h Pac i f i c ( E N P ) • La u r san d L y n n (1 975 , 

1977) indicated that the character and position of the Transition 

lone, directLy or indirectLy, influence the offshore distribution 

nd migration routes of aLbacore tuna movin q from the central 

orth Pacifi~ into the summer fishery off the continental west 

coast. 

SeLected verticaL sections ~f the data have been published 

~onthLy in Ei~hiQg IQf~cm~tiQQ 3 since March 1972. Interpreta- ions of features in the sections were included through March 

1975 (Saur 1972-75). Saur et ale (1979) discussed t he characteristics of long-term mean vertical sections of subsurface 

temperatures trom the XBT data on the San Francisco route. 

IScripps Institution of Oceanography, La Jolla, CA 92037. 

2Pacific Environmental Group~ NationaL Marine Fisheries Service, 

c/o Fleet Numerical ~eather Central, Monterey, CA 93940. 

3Sout hwest Fisheries Center, NMFS, NOAA, La Jolla, CA 92037. 
Paper 7 

In this report we present distributions of surface salinity, sea 

surface temperature (SST), and heat storage (surface to 100-m 

Layer) during 1976, and have extended the previously published 

1972-75 time series of their anomalies through 1976. We discuss 

the 1976 distributions and differences in anomalies from the 

preceding years. An apparentLy atypical reLation of positive 

temperature anomaLies occuiring with negative saLinity anomalies 

off the Pacific coast during October-December 1976 is attribu ted, 

at least partialLy, to a decrease ln evaporation and weak 

vertical mixi~g by winds. 

OBSERVATIONS 

ObservationaL programs and ~rocedures tor making XBT observations 

aboard cooperating merchant shiDs have been described by Sau r and 

Stevens (1972). The "surface" salinities a re determined from 

water samples drawn at arouna 7 m below the surface. " Surface" 

temperatures from the XBT observations are representative of 

temperatures at about 5 m. Heat storage is p r esen ted as average 

temperature from the surface to 100 m as determined from the XBT 

observations. Th~se observations were normalLy scheduLed at 4-h 

intervals. 

For 1976 the number of ship of opportunity 

observations, and range of observed 

Table 7.1. 

TabLe 7 .1 

Number of 

Transits Obs . 

Surface salinity (0/00) 27 81 4 

Surface temp. (C) 31 926 

Heat storage ( C, 0-100 m) 30 868 

trarlsits, 

vaLues are 

number 

sho wn 

of 

in 

Minimum Maximum Range 

32.37 35 .59 3.22 

10. 0 25.9 15 .9 

10 .0 25.2 15 .2 

The locations of the observations are shown in Figures 7.2-7.4. 

In these, and other figures, the location of an observation is 

given by its great circle distance from a reference point, 

21N121, 157W4Z ' , which is in the ocean channeL near Honolulu, 

south of Mckapuu Point, Oahu. 
Paper 7 

DISTRIBUTION OF VARIABLES DURING 1976 

The time-space distributions of salinity, temperature, and heat 

storage (0-100 m) are shown in Figures 7.2, 7.3, and 7.4, respe'ctively. The irregularly located observations were first analyzed 

by the NORP,AX/SURFACE II computer program to a time-space grid of 

24 intervals per year by 92.6 km (50 n mil. The distributions 

were then c~mputer contoured from the Uo~mQQtb~g grid fields 

using double Linear interpolation with five subintervals within 

each standard grid interval. 

The surface salinities (Fig. 7.2) showed the underlying mean 

pattern (Saur 1978) of a low salinity minimum (below 33.0 0/00) a 

short distance offshore in the California Current; a region 

where salinity increased toward Hawaii and had maximum gradients 

located between 2,000 km and 3,000 km along the route from 

Hawaii; a region of maximum salinites (above 35.0 0/00) located 

between 500 km and 1,750 km from Hawaii; and somewhat lower 

salinities (below 35.0 0100) most of the year near Hawaii. The 

high salinities occurred where the vessel track crossed the 

eastern end of the high salinity Eastern North Pacific Central 

Waters, located between 2sN and 30N (Sverdrup et ale 1942). 

The surface. temperatures (Fig. 7.3) showed the typical annual 

cooling and warming cycle with minimum temperatures in late March 

or early April and maximum temperatures in September superimposed 

on the l at it. u din a l dec rea s e i n t e m per at u r ea l 0 n 9 the r 0 ute fro m 

Hawaii to San Francisco. The most rapid warming normally occurs 

from mid-May to mid-July, but in 1976 the warming was delayed 

until mid-June and was greatest in July. This was followed by a 

broad maximum through October and slowly decreasing temperatures 

in November-December. 

The annual cycle of temperature is much more prominent than the 

annual cycle of salinity. Minimum and maximum values and total 

range for each gridded field are shown in Table 7.1. The 

greatest range of salinty at a given position was about 0.5 0/00 

or only 15% of the total observed range. On the other hand, near 

the California coast the temperature range was 6.0C, and near 

3,000 km along the route (in the Transition Zone) the annual 

range was 5.1C, which were 39% and 32%, respectively, of the 

tot a lob s e r v ed ran g e • 

The heat storage (expressed by the average temperature in the 

upper 100 m of water, Fig. 7.4) had a pattern similar to that of 

surface temperature. However, at a fixed location it did not 

have as large an annual range; thi~ was only about 2C over most 

of the route hut reached about 4C near the California coast. The 

smaller annual range of heat storage occurred because the effects 

of the seasonal warming and cooling cycle decrease with depth. 
P a pe r 7 

ANOMALIES DURING 1976 

The time serie s since 1972 of anomaLies of ' saLinity, temperature, 

and heat s tor age g i ven by Saur (1~78) are extended to incLude 

1976 anoma i~s (Fi g . 7. . 5 ). The mean data from which the 

anomaLies we r e compute d did not incLude the 1976 data, but were 

for the sa me 8-y r per i od (June 1966-December 1970, January 

1972-June 1 97 5 ) used prev i ousLy. The grid fieLds for the 

anomaLie s we re n um erica LLy s moot hed by a 5 x 3 point (60 days by 

100 n mi) befQre bei ng contoured. 

The anomaLi e s of surf ace saLinity we re generaLLy smaLL, but 

dominantLy positi ve , thr oughout t he f i rst nine months of 1976. 

Two exceptions a re no t iceabLe. ALo ng t he CaLifornia coast there 

was a puLse of beLow normal salini ty water in January-February 

and another in May - JuLy. Ne a rer mid sec t i on the negative anomaLy 

( -0. 2 0/00) which had appeared nea r 2,7 00 km in Late summer 1975 

mi g ra ted westward a Long the track, decr eased to near normaL in 

wint er, but then increased in inte nsity to -0.2 0100 around 

2, 000 km in May and June 1976. This pr opag ation speed aLong the 

rout e was about 3.3 cm/s as compar ed wit ~ observed vaLues of 

2.5 cm/s in 1972-75 and speeds of 2 . 9 cmls for temperature 

anoma lies at 170 m (generalLy in the thermo cLine) found by Dorman 

and Saur (1978). 

The outstandiog feature of surface saLin i ty anomalies in 1976 was 

the appearance of significant nega tive anomaLies (beLow 

-0.2 0 /00) at the California coast and aLso near the outer edge 

of t he CaLifornia Current (near 2,800 km ) in October~ In midNov ember there was a band of negative a no ma Lies (beLow -0.3 0100 ) 

fr om near the CaLifornia coast to mids e cti on. Further, anomaLie s 

beLow -0.4 0/00 occurred in the Transitio n Zane and extende d 

tow a rd Hawaii somewhat into th~ ENP r egion. The s e stron g 

nega tive anomaLies appeared to be return ing to near nor maL at th e 

e nd of the year. 

The SST anomaLies in 1976 exhibited th e earLier observe d coherence wit~ distance aLong the track an d Low persistence in time. 

From January through ApriL tempereture ano maLies were positive 

ov er most of the route except that they were negative within 

a bo ut the Last 600 km approaching the CaLifornia coast. A change 

to significantLy negative anomaLies occurred in May over the 

entire route because of the previousLy mentioned deLayed onset of 

seasonaL warming. Warming in JuLy bri efLy returned t he anomaLies 

to near zero aver most of the route. A narrow band of positive 

anomalies appeared near th e CaLif or ni a coast at that time. The 

anomaLies over the re st of the r oute returned, however, to 

significantLy negati ve va Lu e s during August through October. 
Paper 7 

During the last quarter, positive temperature anomalies appeared 

progressively farther westward along the route towards Hawaii at 

a very rapid rate. Significant rositive anomalies <above O.5C) 

appeared during November over the entire eastern half of the 

section and persisted through the remainder of the year. The 

pattern of these positive anomalies was quite similar to that of 

the negat~ve salinity anomalies that ~ere previousLy noted. 

The pattern of anomalies of heat storage in the upper 100 m 

aiffered considerably from that of surface temperature anomalies. 

Only during the first quarter of the year was there some 

correspondence of positive anomaLies of heat storage and surface 

temperature over most of the route along with negative anomalies 

near the California coast. During May-July over the central 

portion of the route, the positive anomalies of heat storage 

persisted while the anomalies of SST changed to negative, indicating that the warm waters remained at depth but were covered 

with anomalou&ly cooL waters at the surface. 

Toward the last haLf of the year negative heat storage anomaLies 

progressively appeared over a larger portion of the route at the 

Hawaiian end of the section. Otherwise, the patterns of significant heat storage anom?lies were very spotty. 

DISCUSSION 

The oceanic conditions in 1975 on the San Francisco-HonoluLu 

route began with the relation between surface salinity and 

surface temperature anomalies which has been typical for at least 

the period 1972-75. This historical reLation had banded and westward-migr~ting positive (or negative) salinity anomalies over 

the eastern half of the route accompanied by positive (or 

negative) surface temperature anomalies over most of the route. 

This relation continued in the first quarter of 1976 when 

positive saLinity anomalies were associated with positive 

temperature anomaLies. 

During midye~r the relation broke down and 1976 ended with a 

strongly atypical relation between saLinity and temperature 

anomalies. Negative salinity anomalies occurred simultaneously 

for 1,500 km aLong the eastern part of the route with positive 

temperature anomalies--a reversal from the previous relation. 

For the years 1972-75 an heuristic model with anomalies dominated 

by advective processes could expLain the association of positive 

salinity anomalies in the outer California Current region with 

wider spread positive temperature anomalies. The California 

Current is the fastest portion of the eastern limb of the major 

(clockwise) gyre of the central North Pacific. Along the 
Paper 7 

San Francisco-Honolulu route th av r e curr n flow fro 

northwest to southeast , esS nti lly normal to th rout A 

increase in speed of the Jorth Pncific yr would brin in mor 

cool, Low saLinity , modified ub rctic t r which, on the route, 

would appear first in the California Cu rr nt r gion and Later in 

the Transition lone. This wouLd r _s ult in Rare np c tive s linity 

and temperature anomalies in thesp r eas . Over the w st rn half 

of the route, dn incre~se in p ed of h nyr woul al 0 r ul 

in increasingLy negat;vp tem er ture nomaLi s (due to meri ional 

gradients of temperatur) ou t wnul not r S Lt in i nif1cant 

negative salinity ~nomaLies because me ri diond L sa linity gr ients 

::Ire weak or nonexist nt in that dre ( R i 1 6 ). The ;ncreas 

(or decrease) in sp ed of the gyr co ld r s lt fro Lon -ter 

forcing by winds. This simple L ss m s that thp variability 

from heat exchange and v rticaL mixinn n g Li gib l p • 

t 

The patterns ~f saLinity and t eratur 

this modeL in tre last tree m nt IS f 

(Pape r 2) noted that during 1976 th 

also chan ced noticeabLy. Du rin 

anoma lous circuLation was stron~ly 

Pacific. But during the last r e 

established itseLf over the este rn 

div r d redtLy fro 

7b . Dic son and :a 

pr ai r ( 700 b) att 

e 'first thre e sea ons 

l ac r oss the central' ort 

t , a i h ressure ridoe 

acif,c and we t coast 

r an 1 76-77 _inter 

documpnted in the 

of No rth America. The ens~i~Q fair we at 

drought over the western United States re 

~QQlhly ~~£lb~[ ~~~i~~. ~ 

The breakdown in Cctober thro h Oece ber 76 of the earlier 

relation between salinity and tem era u r e anomaLies indicated a 

change in balance of oceanic rocesses. If we consider tha 

surface saLinity is a uasi-conservative ro pe rty and the lo 

anomalies were due to increased advection to the south, we us 

Look for processes that 'ouLd Change a ne ga tive temperatur 

anomaly to positive. The possibiLity t at increased anomalou 

heat exchange and less vertical mixing by weaker winds contri 

buted to positive anomalies was explored using onthly mean dat 

compiled by 5-deq quadrangles at the So uthwest Fisheries Center 

AnomaLies wer~ computed for two quadrang les for the last thre 

montrs of 1974, 1975, and 1976 (TabLe 7.2). One of th 

quadrangles <35N-40N, 125w-13010 lies over the California Curren 

west of San Francisco and is crossed by the ship route. Th 

other (40N-45N, 125N-130W) is the adjacent Quadrangle to th 

north, throu~h which waters normally fLow before crossing th 

route. Heat excrange anomalies ~ere computed from the 1961-7 

me2ns given by Clark et ale (1974). Wind speed anomaLies wer 

computed from the 1961-76 monthly means published in 1976 issue 

4 Professi onaL journaL of the American 

Vol. 105, Nos. 2-5, February-~ay 1977. 

r·1eteorological Society 
The anomalies showed that wind speeds were lower and heat gaine 

by the ocean was much hi ghe r in 1976 than in the previous two 

years. The decreased wind speeds along with occurrence of warm, 

moist air resulted in less evapor ation and sensible heat loss 

and, consequently, more heat rete~tion by the ocean (Table 7.2>. 

Decreased wind speeds also permitted more stratification in the 

ocean and thu~ a greater positive surface temperature anomaly 

from the excess heat gain. 

The major characteristics 

Table 7.2 are: 

of anomalies which stand out 1 n 

1) In both quadrangles there was a month to month consistency 

of ~eat exchange anomalies in 1976, particularLy as com~ared 

with 1974. The same consistency occurred in the anomaLies 

of wind speed. 

2) Above normal retention of heat by the ocean because of 

reduced evaporation was the major component in 1976. Above 

normal incoming radiation and lower flux of sensible heat 

were secondary terms. Year to year changes of effective 

back radiation were relatively s~all. 

3) The total heat flux anomaly ir 1976 , the anomaly from 

decreased evaporation, and the wind speed anomaly were 

larger in magnitude in the area to the north of the route 

(upcurrent) than in the immediate area of the XR.T observations. 

The data presented in Table 7.2 indicated that processes (heat 

exchange and vertical mixi ng) previously considered smalL as 

compared with advective processes Jere, at least partiaLly, 

responsible for the late 1976 reversal of the relation of 

salinity anomalies to temperatur e ano~alies observed in 1972-75. 

We are mindful that this argument is based on the assumption that 

the salinity anomalies resulted from advection and that the 

temperature anomalies were atypical. It ;s not im ediateLy 

apparent how one could interpret the data if the temperatur 

anomalies were assumed to be advective and it were necesssary to 

explain the salinity anomalies as atypical. 
Paper 7 

ACKNOWLEDGft1ENTS 

We thank the Chevron Shipping Co. and Matson Navigation Co. for 

their cooperation and tt'Jat of their ships ' personnel in making 

the observations used herein. The FLeet Numerical Weather 

Central supplied the XBT nrobes and the use of computer 

facilities at Monterey. 

This project was a part of the NORPAX program and was supported 

by grants from the National Science Foundation , Office for the 

In~ernational Decade of Ocean Exploration. 

LITERATURE CITED 

CLARK , N. E., L. E. EBER, R. M. LAURS, J. A. RE 

S AU R. 

Ef~ , and J. F. T. 

1974. Heat exchange between ocean and atmosphere in 

eastern North Pacific for 1961-71. U.S. Dep . Commer., 

Tech. Rep. NMFS SSRF-682, 1GB p. 

DORMAN, C. E., and J. F. T. SAURo 

the 

OAA 

1973. Temperature anomalies between San Francisco 

lulu, 1906-1974, gridded by an objective anaLysis. 

Oceanog. 8:247 -257. 

and Hono -

J. Phys. 

LAURS, R. M., and R. J. LYNN. 

1975. The association of ocean bo~ndary features and aLbacore 

tuna in the ~ortheast Pacific. !n Proceed ings : Third S ITID 

Conferen~e and Workshop, San Diego, CA, p . 23 -3 0 . 

1~77. Seasonal migration of North Pacific albacore, Ih~Qn~! 

~l§l~QgQI into North American coastaL waters: Distribution, 

relative abundarce, and rtssociation with Transition Zone 

waters. Fish. Bull. U.S. 75:795-t22. 

REID, J. L. 

1969. Sea-surface temperature, salinity, and density of the 

Pacific Ocean in summer and in winter. Ceep-Sea Res. 

1t(Suppl.):215-224. 
iAUR, J. F. T. 

1972-1975. Subsurface temperature structure in the northeast 

Pacific Ocean. fi~hina !niQCID[tiQQ (monthly), NOAA, NMFS, 

Southwest Fisheries Center, La Jolla, CA 92037, 1972(11-12), 

1973(1-12), 1974(1-12), 1975(1-3). 

1978. Oceanic conditions between the Hawaiian Islands and the 

U.S. West Coast as monitored by ships of opportunity - 1975. 

1Q J.~. Goulet, Jr. and E. D. Haynes (editors), Ocean 

variabity: Effects on u.S. marine fishery resources - 1975, 

p.151-168. u.S. Dep. Commer., NOAA Tech. Rep. NMFS Circ. 

416. 

;AUR, J. F. T., L. E. EBER, D. R. McLAIN, and C. E. DORMAN. 

1979. Vertical sections of semimonthly temperature on the 

San Fran~isco-Honolulu route: From expendable bathythermograph observations, June 1966-December 1974. u.S. Dep. 

Commer., NOAA Tech. Rep. NMFS SSRF-728, 35p. 

>AUR, J. F. T., and P. D. STEVENS. 

1972. Expendable bathythermograph observations from ships of 

opportunity. Mar. Weather Log 16(1)1-8. 

>VERDRUP, H. ~., M. W. JOHNSON, and R. H. Fleming. 

1942. The oceans: Their physics, chemistry, and general 

biology. Prentice-Hall, Inc., N.Y., 1087 p. 

85 
Figure 7.1.-Three oceanic domains (schematic) in the eastern North Pacific Ocean crossed by 

cooperating merchant ships taking surface salinity and expendable bathythermograph observations 

during 1976. Observations reported herein were taken on the San Francisco to Honolulu route (solid 

line). 

86 
0 Surface Salinity (% 0) 0 0 co (J ,...., en 

u 

c 

0 0 '- 0 l..L. E 0 

,...., c ~ 

0 

en <U 

<J 

c: 

0 

in 

(5 § 

N 

<U 

<J 

~ 

U 

- 0 0 0 <U 

~ 0 

(.!) 

:;:) 

:;:) 

0 

C 

0 

I 0 

J 

1976 

Figure 7.2.-Surface salinity in parts per thousand (%.) between San Francisco 

and Honolulu during 1976. Symbols (+) indicate the locations of observations in 

time and distance. Contour interval is 0.25% •. 

87 
v 

:J o 

('\j 

o 

v 

D 

v 

:J o 

('\j 

C) I+--~~ 

I 

V 

o 

o 

x 

o ~ 

(/) 

W 

-.J 

« 

2 

o 

z 

« 

>-

fZ 

-.J 

<! 

(/) 

w 

u 

~ et: 

:::J 

t 

(/) ~~~~~~~~ 

008£ 000£ OOOZ 0001 0 

(Wl\) ilJUOIS10 illJJIJ IOilJ9 

O::>SI::>UDJ.::J UDS 

90 

v 

~ ] 

u 

o 

(/) 

W 

-.J 

<! 

:2 

o 

Z 

<! 

W 

et: 

:::J 

~ et: 

W 

Cl.. 

:2 

w 

fW 

U 

~ et: 

:::J 

(/) ~~~~-4~~L4 

008£ 000£ 0002 0001 o 

(WIj) ilJUOIS10 illJJIJ IO ilJ9 

O::>SI::>UDJ.::J UDS nlnlouoH 
<.0 

,.... 

0 0 HEAT STORAGE ANOMALY ,6T ;/IOOm (OC) u 0 (/) ~ co 

~ 3: >\--·~~~~tb LL '" 8 ~~:: 0 i ~ 

if> 

§ 

.,,0 ~ J'.-

-::~~ ~C ~ 

o 8 ~ 0 0 '" N I 0 

:g 0 -;) 8 ~>-

.2 

Uo 

0 Q "; 

\ 

(') 

~ 

c ~ iCcJ> -8 ~ .; -) / 0\ ,,+ 

§ 0 

I 1972 1973 1974 197 5 1976 

Figure 7.5.-Anomalies on the San Francisco-Honolulu route. ,Januar) 1972-Deccmber 1976. \naly,e, in all three panch were smoothed before con touring (see text). Uppe r : Sa -

linity a nomalies; labels on contours are the anomaly multiplied b) 10. Center: Sea .,urface temperature anol11alies; contour interval is o.se. Lower: Heat storage a noma lies for 

the surface to 100-111 la)er, expre,sed a, departure from the mean of a\erage temperature (T) 0-100 III in degrees Celsius. 
co 

r-:> 

TABLE 7.2. Anomalies of heat exchange (cal cm- 2 d-l ) and of wind speed (knots) at two 5-degree quadrangles 

in the California Current Region. Quadrangles lie a) on San Francisco to Honolulu ship route and b) upcurrent from route. positive (negative) values indicate anomalous heat gain (loss) by the ocean. 

1974 3-mo 1975 3-mo 1976 3-mo 

Oct Nov Dec mean Oct Nov Dec mean Oct Nov Dec mean 

o 0 0 0 On route (lat. 35 -40 N, long. 125 -130 W) : 

Incoming radiation 19 -4 9 8 -12 3 -18 -9 7 3 23 11 

Effective back radiation -10 -6 1 -5 7 -7 19 6 -3 -6 -10 -6 

Evaporation -3 -58 26 -12 -18 -40 54 -1 13 19 17 16 

Sensible heat flux -4 -16 13 -2 10 -4 14 7 1 -3 11 3 

Total (net) heat flux 2 -84 49 -11 -13 -48 69 3 18 13 39 23 

Wind speed (knots) anomaly -1 -2 o -1 1 1 -1 0.3 -3 -3 -2 - 2.7 

o 0 0 0 Upcurrent from route (lat. 40 -45 N, long. 125 -130 W) : 

Incoming radiation -3 -10 4 -3 -20 11 -10 -6 20 15 17 17 

Effective back radiation 13 -9 6 3 18 -3 16 10 1 -') -5 -2 

Evaporation 57-73 39 8 8 22 60 30 44 35 61 47 

Sensible heat flux 17 -31 2l:l 4 ')1 12 15 1 18 15 24 19 

Total (net) heat flux 84 -12 .. 76 11 21~ 43 81 50 82 63 '.) 80 

Wind speed (knots) anomaly -1 4 -1 0 . 7 4 2 -1 1.7 -2 -3 -5 -3.3 
Pa oer 8 

THE 1976 EL NINO ~ND RECENT PROGRESS 

IN MONITORING AND PREDICTION 

Willi~~ H. Quinn 1 

INTRODUCTION 

In earlier papers, the author (Quinn 1974, 1976) presented ~efinitions and concepts regarding the El Nino phenomenon and a 

ethod of predicting its occurrence utilizing Southern 

Oscillation (S.O.) indice s (p ressure differences between sites 

representing the Indonesia n equatorial low and South Pacific 

subtropical high) and other variables. In 1975, Quinn (1978) 

predicted the 1976 El Nino type event. The prediction was 

verified by an event of moderate intensity, and indications from 

data are disc~ssed here. 

New methods of handling pressure indices and other variables for 

monitoring and predicting El Nino are presented in this paper. 

CHANGES IN FILTER AND DATA APPLICATIONS 

In earlier papers the 12-mo running mean filter was app l ied to 

s.o. in0ices in order to bring out interannual fluctuations. 

However, in 1276 a switch was made to the triple 6-mo running 

mean filter (involving three successive passes of the 6-mo 

running mean over the involved data); and this was applied to 

anomalies of pressure difference (with anomalies obtained by 

subtracting long-term monthly mean values of pressure difference 

from the individual monthly values) to show the interannual 

changes (Figs_ 8.1a and 8.1b). Since three mon th s of time are 

lost with each successive application of the 6-mo running mean, 

we also use the less-smooth 3-mo running mean plot of index 

anomalies to guide our assessments and outlooks. The same te~hniques are applicable to data for other variables. 

Figure 8.2 shows plots of pressure index, sea surface temperature 

(SST), sea level, and rainfall anomalies for near equatorial 

lSchool of Oceanography, Oregon State University, Corvallis, OR 

97331. 
Paper 8 

sites that reflect the interannual changes discussed in this 

paper. Due to the large month to month variations in pressure 

and rainfall, a higher degree of smoothing was applied to their 

anomalies in this illustration. 

The El Nino (tN) type activity sets in pr ior to and/or in 

conjunction with the relaxation troughs following anti-El Nino 

peaks in the anomalies . The intensity of such even ts depends not 

only on the degree of relaxation but also on the time of year 

that it occur~. The stronger cases [denoted by EN ( S ) and EN(M) 

in Figs. 8 .1a and 8.1b for strong dnd moderate , respectively, 

El Ninos] occurred when the i~terannual relaxation was large and 

indices conti~ued to fall rapidly through t~e early mon ths of the 

year so 2S to reinforce the re guLar seasonaL reLaxation of the 

southeast trade system (Southern Hemisphere summe r season). 

C?ses where the interannuaL reLaxation ~as too smalL, or it 

occur red too earLy or too Late to folLow throug h the seasonal 

reLaxation period, resulted in weaker L ino events . 

The studies ot Be rLa ge (1957, 1~66) and Troup (1965) indicated 

that the s.o. affected not onLy the Sou tr Pacific subtropical 

high but also the orth Pacific subtropicaL hi gh region. This 

reL~tionship ~as explored su~erficiaLLy in Quinn and Zopf (1975); 

howeve r, in that case the Easter Island componen t was compared to 

the former Ship N Locati on component using the 12-wo running mean 

fiLter. Here we consider Rapa, AustraL IsLands, in relation to 

the old Ship N po~ition, because it is much nearer the same 

Longitude, ana use the smoother triple 6-mo running mean filter 

on the index anomalies. A maximum correLation of 0 .59 at no Lag 

was obtained in this case. (This is ~eLL within the 1% 

confidence level.) Figure b.3 co~pares the Rapa-Darwin index to 

the Ship N-Dar~in index. (The plots are correlated at 0.80 . ) 

From visuaL inspection one cnn see there is no consistent 

lead-Lag relationship between the two index tre ndS ; in one cas 

the change in trend wiLL show up first sou th of the equator an 

in another it will show up first north of the equator; 

nevertheless, it is evident that the two high pressure areas ar 

being similarly affected by the S.O. In the future, indications 

from the Ship N-Darwin index wilL aLso be actively considered fo 

outLooks on EL Nino and eouatoriaL Pacific activity. 

USE OF SEP SURFACE TEMPERATURE TRENDS 

A cLose relationship of fLuctuations in north equatorial 

countercurrent transport and resuLting sea surface temperature 

(SST) anomalies off the coast of Central America (illustrated in 

fig. 2 of Wyrtki 1973) to the interannual variations in southeast 

trade strength (as refLected in the 12-mo running mean trend of 

the S.O. inde~), was noted in Quinn (1974). In a recent climatoa 
Paper 8 

LogicaL investigation of the southeast part of the North Pacific, 

time series pLots of SST were studied for several Marsden Square 

eMS) quadrants in order to find particularly suitable areas for 

diagnosing ch~nges associated with the El Nino type developments. 

Figure 8.4 sbo~s two of the quadrants selected; MS 10(1) 

reflects changes taking place along the equator, and MS 10(3) 

reflects changes in an area affected by the north equatoriaL 

countercurrent. Figure 8.5 shows how the Easter-Darwin index 

anomaly trend reLates to SST anomaly trends for MS 10(1) and 

MS 10(3) when the data are subjected to the triple 6-mo running 

mean filter. MS 10(1) is next to the equator, and when the 

circulation is relatively strong (S.O. index is high) it shows 

lower SST's due to the advection of cooler Peru current water 

into the area and /or equatorial upwelling; when the circuLation 

is weak (index is low); SST's rise. MS 10(3) SST's reflect 

changes in the north equatorial countercurrent transport 

discussed early in the section. Table 8.1 shows lag correlation 

coefficients between index and SST anomalies. Changes show up 

about a month earlier in the index than in the MS 10(1) SST trend 

and about three months earlier than in the MS 10(3) SST trend. 

Events of significant magnitude are reflected in both the index 

and SST trends of Fig. 8.5. The value of the corroborative SST 

evidence is shown in 1961, when the indication of a fairly deep 

Easter-Darwin index trough was not substantiated in the SST 

trend. Since this trough was of much less significance in the 

other index trends of Fig. 8.1a, an unrepresentatively low Easter 

input was the misleading factor in this c ase. As an interesting 

sidelight, Berla~e in 1960 put out a wi dely pubLicized forecast 

f or an El Nina in 1961 (Schweigger 1961). However, there was no 

significant El Nino development in 1961. A compar i son of the 

Easter-Darwin index anomalies with anomalies of the other indices 

a nd the ~S 10(1) SST anomalies would have precluded the forecast. 

Th ree-month running mean plots of the index anomalies and the SST 

a nomalies for MS 10(1) (Fig. 8.6) become particularLy useful to 

t he forecast process between 18 and 3 months prior to the onset 

o f El Nino. However, they should also be followed closely during 

t he course of an event to determine whether a subsequent 

s econdary trough in the index is likely or a persistent recovery 

f rom the initial event is probable. 

THE 1976 EL NINO EVENT 

I n summer 1975 an outlook for El Nino type activity in 1976 was 

prepared. The outlook was given at the October 1975 Eastern 

Pacific Oceanic Conference and at several subsequent meetings, 

workshops, and seminars. The 12-mo running mean of the EasterDarwin index was predicted to rise from the shaLlow earLy 1975 

trough to a small peak by the middLe to latter part of 1975 and 
Paper 8 

then to falloff to a deeper trough in 1976. The analog selected 

for this development was the 1964-65 situation. (There was a 

rise from a shallow index trough in late 1963 to a small peak in 

mid-1964, then a fall to a deep trough in 1965 when an El Nino 

occurred.) Heavy western equatorial Pacific precipitation was 

called for in the latter half of 1976-early 1977. 

The expected &mall peak in the interannual index trends occurred 

in late 1975 and there has been a falling trend since then (Fig. 

8.1b). Figura 8.5 shows the corroborative rise in SST anomalies 

3S the index fell. Figure 8.6 shows the deep 3-mo running mean 

trough in indax anomaly and the associated large peak in SST 

anomaly for MS 10(1). Figure 8.7 shows the positive SST 

anomalies off the coast of Peru and southern Ecuador extending 

westward over the equatorial Pacific. Table 8.2 shows the SST 

and SST anomalies for two stations along the coast of Peru during 

1975-76, and Table 8.3 shows precipitation at Guayaquil, Ecuador, 

during the la&t three El Nino events. (The 1972-73 case is 

considered to be strong, 1975 very weak, and 1976 moderate in 

intensity.) Tarawa, Gilbe rt Island~, data have been used to represent the western equatorial Pacific rainfall; and the triple 

6-mo running mean trend of the rainfall anomalies clearly shows 

the rainfall peak (Fig. 8.2). For the period April-December 1976 

the rainfall was 1,130 mm above normal and it is expected that a 

few more months of this heavy rainfall will occur in early 1977. 

El Nino evidence indicated that the forecast for the 1976 event 

was accurate as to time of occurrence and intensity <similar to 

the selected 1965 analog). Figure 8.2 shows how trends of variables at various locations were affected by this recent El Nino. 

FURTHER OUTLJOK 

In the summer of 1976, the further outlook to the Coastal Upwell 

ing Ecosystem Analysis <CUEA) Peru project called for a hold-ove ~ 

of the 1976 positive SST anomalies through February 1977 along 

the Peruvian coast, with a return to near normal coastal SST's by 

March or April 1977. The analog given for the 1976-77 holdover 

effect was the 1965-66 situ~tion; however, the 1976 onset was a 

month or two later (than in 1965) and the lag effect in 1977 was 

also expected to be a month or two later (than in 1966). 

In retrospect, Wyrtki et al. (1976) reported that a patch of the 

warm water that crossed the equator in the southward 

transgression of early 1975 had been cut off and remained south 

of the equator. MonthLy SST analyses 2 showed this warm body of 

2£i ~hiDg IniQrm2!iQQ' 1975 and 1976, Southwest Fisheries Center, 

NMFS, NQAA, La Jolla, CA 92038. 

----______ O 
P ape r 8 

water to remain west of Peru through the rest of 1975 and on into 

1976. This residual effect along with the event triggered by 

large-scale relaxation in the southeast trade system between late 

1975 and mid-1976 [as characterized by the falling indices 

following the late 1975 pecks (Fig. B.1b)] most likely caused the 

1976 El ~ino to appear as it did. 

CONCLUDING REMARKS 

Large-scale climatic patterns, as welL as fluctuations in 

oceanographic conditions in the eastern tropical Pacific and 

particuLarLy in the Peru fishery region, appear to be closely 

associated with the s.o. We have found that to a large extent we 

can use trends in s.o. indices to anticipate extremes in the 

fLuctuations and provide outlooks for environmentaL change. We 

hope in the future to substantially improve our abiLity to 

predict cLimatic changes and to be able to roughly assess their 

environmental impact so that plans can be set in motion to 

minimize effects on the fishery. However, fishery management 

must be capable of using monitoring and prediction data to 

establish sujtable fishing practices. So far this has not been 

the case. In both 1972 and 1976 the main fishing season 

(March-May) proceeded witnout considering an El Nino that was 

aLready under~ay; and in both cases it could be argued that the 

reproductive stock should have been con serv ed so as to minimize 

the recruitment failures in 1973 and 1 97 7. 

ACKNOWLEDGMENTS 

I thank the Director of the Civil Aviation Service and the Chief 

of the Metenrological Service of Polynesie, Francaise; the 

President of the Instituto del Mar deL Peru; the Director of the 

Australian B~reau of Meteorology; the Director of the Hydroqraphic Institute and Chief of the Naval Weather Service of the 

Armada de ChiLe; the NationaL CLimatic Center, EnvironmentaL 

Data Service, NOAA; the Pacific EnvironmentaL Group, NationaL 

~arine Fisheries Service (NMFS), NOAA; and the Southwest 

Fisheries Center, NMFS, NOAA for their invaluabLe support to this 

study. I am greatLy indebted to Forrest R. MiLLer of the 

Inter-American TropicaL Tuna Commission and Richard Evans of the 

Southwest Fisheries Center for timely information on sea temperatures and weather conditions over the eastern tropicaL Pacific 

and to Jose M. Diaz-Andrade, Universidad, Costa Rica for the 

Quepos sea level data. I also thank Kent Short, now with the 

Western Reoion (SeattLe), ' National Weather Service, NOAA, and 

CLayton Creech and David Zopf ~f the School of Oceanography, 

Oregon State University, for their active participation in this 
Paper 8 

project. Support by the NationaL Science Foundation under the 

North Pacific Experiment of the International Decade of Ocean 

Exploration through NSF Grant No. OCE 75-21907 A01 and under the 

Climate Dynamics Program of the Division of Atmospheric Sciences 

through NSF Grant No. ATM 77-00870 is gratefully acknowLedged. 

LITERATURE CITED 

BERLAGE, H. P. 

1957. Fluctuations of the general atmospheric circulation of 

more than one year, their nature and prognostic value. Mededel en. Verhandel., No. 69, Kon. Ned. Meteor. Inst., 152 p. 

1966. The Southern Oscillation and world weather. Mededel. 

en Verhandel., No. 88, Kon. Ned. Meteor. Inst., 152 p. 

QUINN, W. H. 

1974. Monitoring and predicting El Nino invasions. J. A~pl. 

Meteor. 13:825-830. 

1976. El Nino anomalous equatorial Pacific conditions and 

their prediction. In J. R. Goulet, Jr. (compiler), The 

environment of the United States living marine resources- 1974~ p. 11-1--11-18. u.s. Dep. Commer., Natl. Oceanic 

Atmos. Admin., Natl. Mar. Fish. Serv., MARMAP (Mar. Resour. 

Monit. Assess. Predict. Program) Contrib. 104. 

1978. Equatorial Pacific anomalies and El Nino. 10 J. R. 

Goulet, Jr. and E. D. Haynes (editors), Ocean variability: 

Effects on U.S. marine fishery resources - 1975, p. 179-190. 

U.s. Dep. Commer., NOAA Tech. Rep. NMFS Circa 416. 

QUINN, W. H., and D. O. ZOPF. 

1975. The Southern Oscillation, equatorial Pacific anomalies 

and El Nino. Geofis. Int. 15:327-354 . 

SCHWEIGGER, E. H. 

1961. Temperature anomalies in the eastern Pacific and their 

forecasting. Soc. Geogr. Lima, Bolet in 78:3-50. 

TROUP, A. J. 

1965. The ·Southern Oscillation.· 

9 1 : 490 - 50 6 • 

WYRTKI, K. 

Q. J. R. Meteorol. Soc. 

1973. Teleconnections in the equatorial Pacific Ocean. 

Science(Wash., D.C.)180:66-68. 

WYRTKI, J., E. STROUP, W. PATZERT, R. WILLIAMS, and W. QUINN. 

1976. Predicting and observing El Nino. Science(Wash •. , D.C.) 

191 : 343-146. 

QR 
Table 8.1.--Lag correlation coefficients between Easter-Darwin (E-D) 

index anomalies and sea surface temperature (SST) anomalies for Marsden 

Square (MS) 10(1) and Marsden Square 10(3). See Table 8.4. 

- 2 

Lag in 

Months 

-1 (index l ags SST) 

o (no lag) 

1 (index leads SST) 

2 

3 

4 

5 

Period of record 

E-D index and 

SST for MS 10(1) 

- 0 . 693 

- 0 . 732 

- 0 . 755 

- 0 . 761 

- 0 . 748 

- 0.717 

-0. 668 

1948-76 

E-D index and 

SST for MS 10 (3 ) 

-0.588 

- 0 . 636 

-0.672 

-0.694 

-0.702 

- 0.693 

- 0.668 

1949- 76 
...... 

8 

Table 8.2.--Monthly mean sea surface temperatures and anomalies of temperatures (degrees C) for 

Talara and Chimbote, Peru, 1975-1976. See Table 8.4. 

Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec 

Talara 

1975 16.3 18.6 22.4 21. 5 19.8 17 .8 18.0 17.7 18.1 18.1 16.2 17.7 

-4.2 -3.2 +1. 0 +1. 3 +0.6 -0.5 +0.2 +0.1 +0.7 +0.4 -1. 8 -0.6 

1976 20.5 24.4 23.6 21. 4 21. 7 21. 2 21. 2 19.0 18.9 19.5 20.1 20.3 

+0.0 +2.6 +2.2 +1. 2 +2.5 +2.9 +3.4 +1. 4 +1. 5 +1. 8 +2.1 +2.0 

Chimbote 

1975 20.5 21. 0 24.2 21. 2 21.1 18.7 17.6 17.0 16.6 17.0 17.3 18.0 

-0.2 -0.8 +2.0 +0.3 +1. 4 +0.1 -0.2 -0.6 -0.6 -1. 0 -1. 4 -1. 6 

1976 18.5 21. 8 23.5 21. 4 21.1 21.1 20.3 20.0 19.2 19.5 20.1 21. 6 

-2.2 +0.0 +1.3 +0.5 +1. 4 +2.5 +2.5 +2.4 +2.0 +1. 5 +1. 4 +2.0 
Table 8 .3.--Rainfall (nun) at Guayaquil , Ecuador for the indicated months . See Table 8 .4. 

19 72 1973 1975 1976 

Hon t hs Tot a l Departure Total Departure Total De parture Total Departure 

January 220 +9 70 1 +490 2 21 +10 417 +206 

.- February 330 + 45 21 0 -75 48 7 +20 2 586 +3 0 1 0 

- Horch 407 +115 492 +200 60 7 +31 5 450 +1 58 

Aj)ri 1. 143 - 62 181 - 24 202 - 3 182 - 23 

lay 35 - ]9 136 +82 2 - 52 1 44 +90 

J .. me 1')2 +141 3 - 8 4 - 7 10 - 1 
Table 8.4.--Location of stations used in the several 

indices. 

Chimbote , Peru 9S10 ' 78W31' 

Darwin, Australia 12S28 ' 130E51' 

Easter Island 27S1 0 ' 109W26' 

Guayaquil, Ecuador 2S10 ' 79w50 ' 

Juan Fernandez Island 33S37 ' 78W50 ' 

Marsden Square 10 (1) 0-5N 90- 95W 

Marsden Square 10(3) 5-10N 90- 95W 

Quepos, costa Rica 9N25' 84wlO ' 

Rapa, Austral Islands 27S37 ' 144W20' 

Ship N 30N 140W 

Tahiti, Society Islands 17S33' 149W37, 

Talara, Peru 4S34' 81W15 ' 

Tarawa, Gilbert Islands lN22' 172E58' 

Totegegie, Gambier Island 23S06' 134W25' 

102 
...... 

o 

'" 

JUAN FERNANDEZDARWIN (ANOMS. ) 

EASTER - DARWIN 

(ANOMS. ) 

TOTEGEGIE:" DARWIN 

(ANOMS.) 

RAPA - DARWIN 

(ANOMS. ) 

TAHITI- DARWIN 

(ANOMS.) 

4 1948 1949 19~ 19~1 19~2 19~3 19~4 19~ 19!H 4 

3 :3 

2 .......... ..... -t I- 2 .-' ... .. ... . ....... . ...... . 

I

• • .~. • e. .~-~. . 

o . ---. ..- -•• ;-•• - •• ;+--e ....... . . ... ... ......... a.. '--.0 •• -' I . '.-;;-.' • _I •••• -I 

-H-· •• 

.. 

-=t 

0 

-I 

-2 

-3 

2 

0 

i -2 

2 

I 

0 

i

' 

-2 

2 

II-

.. t . 

. . ... 

. . 

. 

. 

... .. -.... 

.......... 

. 0-.. I .' •. -1----, ................ -I 

-2 

-3 

.... 

. ...... . 

.······1··· r····. . . .. ... 

•••••• I • . .... . ....... . . . ... 

.. . .. - '. .' 

. . . . 

a. .- ...... 

....... 

• a. I • 

....... 

. 

. 

.. . 

. 

. 

. ... I I .•...... -+-- .-!.!. I ••••••• ........ ____ 1 

. '-' . • I a. 

. . . 

..... .. .. I·· . . ........ .. --;r----

. ......... . . .. I· .......... . 

....... .......... . . 

I ••••• ..' -., 

. . ... 

.. .. ---. .--. . •• • •••• I ••••• 

...... 

. ............ . • • a •• 

•• . 1 I ...... ... ·· .... 1 . ··r······ .. . . 

. ..... .... I .. --1--- . . . -" 

'. ..' ....... • • I '. 

.... ............. .' -. .- ' . .. - . ••••••• '. ..! .......... I ••••••• • • 

. . 

-2 

2 

o 

·· .. .i-I 

-2 

-3 

2 

.0 

•• •• L.!-I 

-2 

2 

o 

-·-1 

··.!....I-2 

2 

o ..-•• I I.·· .. ···1·1·-·· I ...... r·· 

I 

.' -'. .' a. • •••••• •••• ••••• a • ., a... . . ... . ...... I ...... I •••••••• I • ••• ·j-I 

-2 

-3 

EN(W) EN(M) EN(S)~ EN(W) 

1948 1949 1950 1951 1952 1953 1954 1955 1956 1957 1958 1959 1960 1961 1962 1963 

Figure 8.1a.- Triple 6-mo running means of anomalies of the difference in sea level atmospher ic pressure (mb) between Darwin and Juan Fernandez, Easter, Totegegie, Rapa , and Tahiti. 

El Nino type events (EN) are indicated as strong (S), moderate (M), and weak or very weak (W). See Table 8.4. 
t-' 

~ 

4 1964 1965 1966 1967 1968 1969 1970 1971 1972 1973 1974 1975 1976 1977 1978 4 

3~ I 1 .... r····· .. I.···! .. . . JUAN FERNANDEZDARWIN (ANOMS.) 

2~ 

~.. .. . ............... y .... 

.......... . •• •• ..-. •• •• • I 

O .- •• I '-. .. -..' .. ... . I J (··~ .. f fI r······ .·r···. .... ..... 2~ 

II- ." . . . 

. 

. EASTER - DARWIN 

(ANOMS. ) 

...... I '. . -. or.. _. . e. •••• ..' '1 I ". --+---~. ~---t---

-I r· .... 

--i2 

-3 

2 ••• 

. .' .... . . 

. . 

.... .. -.. . ,-.. 

. . ........... 

TOTEGEGIE -DARWIN 

(ANOMS.) 

I •• •• 

. 

0."'·'---- 1::-. 

.' .......... . 

RAPA - DARWIN 

(ANOMS. ) 

TAHITI- DARWIN 

(ANOMS. ) 

-il 

-2 

2 

. . .' ....... .... 

I ~ •••• . .... . 

-1·- . 

. ~ 

O~· --. I I .:,' •••• ~.... • 

. 

........ . I' . 

. .. ..... . • -I •• . . ..... . . '.' 

I 

r. • .'. • I .. ~'"'' . .. _ ... '...... __ . . I I . . . . . 0.:-... \T .....I I .. ~ ............ . I • I • • -2t 

-3 

- r-- • • . . ....... 

.... . . . ' . '. 

····i·· ....... 

. ··i······· ". . 

. . 

.. 

'.' 

. . 

..... 

-13 

-12 

. . .. I I I I I j~ 

.... 

. '. 

. .' , 

. . 

. ... 

---,. 

. 

..... . 

-I-I 

=f- .... . - " . 

r·· -~---r--~--~O 

•• I· 

. ... 

. 

. 

. ... . . . 

. . " 

... ! .. _--, 

. 

•• I. 

. .... . . 

. .... 

-I 

-2 

-3 

2 

-II 

I I t- -~~--+---~O 

-I 

-2 

2 

---4 I 

--~----+---~----4-----+---~10 

---4 -I 

j -2 

-3 

EN(M) EN(W) EN(S)~ EN(W) EN(M) 

1964 1965 1966 1967 1968 1969 1970 1971 1972 1973 1974 1975 1976 1977 1978 

Figure 8.lb.-Continuation of Figure 8.la. 
s:: 

Triple 6MRM 01 SLP 

Anomalies (mb) 

RAPA- DARWIN 

3MRM 01 SST 

Anomalies (DC) 

CHIMBOTE 

4 19~3 1956 19~1 1958 19~ 1960 1961 I96Z 1963 19" 196~ 1966 1961 1968 1969 1910 1911 1912 1913 1916 1911 4 

3rZr- "'~"'" Z 

or---;:' .... . ..... ~ .............. :: .. :................. :~. .... ..... . ...... 0 

-1\- .: .......... .r·I-1 

-Z-' .... • ..... : ••••• :: ~Z 

II--

o 0 

-I ~ 

-Z -Z 

---1--10 10 

~ ~ 

3MRM 01 Sea LIWel 0 0 

Anomalies (em) -5 -5 

QUEPOS 

--- -10 -10 

Triple 6MRM 01 RClnloll 

Anomalies (mm) 

TARAWA 

~5 ~ 

350 350 

300 

Z50 

ZOO 

150 0 0 :-. . .... ...... 

ZOO 

150 

'r·······!··· ..... t .... ..I. .. J:· .............. ! ........ J .... I. ....... I.. "j," ..... .1 .. " ... .1...... . ..... , ....... ...1 ..... ...1: ··t··· ....... ···:j: :: 

J

: 

100 

50 

~. 

..... 

-ZOO 1953 1954 1956 1951 1958 1959 1960 1961 1963 1964 1965 1966 1961 1968 1969 1910 1912 1913 1974 197~ 1916 1971 -200 

YEARS 

Figure 8.2.-Triple 6-mo running means of anomalies of the difference in sea level atmospheric pressure (mb) between Rapa, Austral Islands, and Darwin, Australia, and Tarawa, Gilbert 

Islands, rainfall anomalies (mm). Three-month running means of sea surface temperature anomalies (degrees C) for Chimbote, Peru, and of sea level anomalies (cm) for Quepos, Costa Rica. 

See Table 8.4. 

• e 

• • ..* : .. ,""o ........... -'!'-

...... ' 

z 

o 

o 

C\J 

o 

o 

, . 

107 

~ o 

o 

CD 

~ 

o 

o 

o 

~ o 

o 

C\J 

..: 

C' 

:: 
..... 

~ 

It--

6 MRM TRIPLE PASS ON 

E-D INDEX ANOM (mb) 0 ·.--t-:----+--4 

6 MRM TRIPLE PASS 

ON SST ANOM FOR 

MS 10(1) (Oe) 

-I 

-2 

-3 

15 

10 

ost--

1952 1961 4 

••••• I .' ..... . ..... . 

j: 

t---+---1--1 -.. ~ .. ~ ... -II-... ··J-~~ ~-I 

..... '-1-2 

~ 

~ 

·············1··············· ..... . 

...... 

•.••• !.. I ..... ,. .......... I 1 10 

-15 •••••• ..' -1.0 

10 ••••••••• -1.5 

6 MRM TRIPLE PASS 05 •••••••• .... I···· 10 ON SST ANOM FOR 0 :T'" ....... .. ....... MS 10(3) (Oe) 05 : ......... _'1'" .. , -.. ~ .. ······1 I ................ 05 _ ..... I ······1 ...... I ~". 0 

•.•.• -•••.•.• I I .... ~-~ ~ -101- -H.O 

2 .. ··r···. .··i·. 

6 MRM TRIPLE PASS ON 

E-D INDEX ANOM (mb) 

~ 3~ ·:1······[··· ~ .... t.-t I ..... I.... '. j.. I 

~, .. .." 

...... 

I •••• ... .:+-J . ~ -I 

. ... 

--1-~.: ... ... (._.... ..····H .. ........ 1 

" ... ;--....- -~ 

=El- I I I" '··1 ......... I I - 15 '.' 

6 MRM TRIPLE 

ON SST ANOM 

MS 10(1) (Oe) 

~~......... :' ". : .. ..... :......... : -

-I~ ~· ·· ' .. _." ......................... : .......................... . .............. _ ...... : -

t-- --LO 

lOt-- - - 15 ..... -

10f . ' -

ost-- ••••• • ". •••• - 10 

6 MRM TRIPL E PASS ............ '. : ••••• ..' ". 

ON SS T ANOM FOR 0 •••• ~~ •• _ : _1--'. .'. .... - 0.5 

MS 10 (3 ) (Oe ) . -05..::. .. ••••••• •••• _..... •••• ......: ". ..... ". 0 -j '. .. ...... '. ..' .... .... . - l Ot-- r' .' '. .... ............ '. .. --05 

. r····· ..... . -15 - 10 

196 2 19 63 1964 I 1965 1966 I 1967 1968 1969 1970 I 19 7 1 1972 1973 1974 1975'! 1976 1.5 

Figure B.5.- Triple 6-mo running means of anoma lies of the difference in sea level atmospheric pressure (mb) between Easter Island and Darwin, Aus-

---------____________ traJ.ia. ancLot ... se:h"urJace. tem.DeJ:a.tm:e..anomalies (.de=ee.s CI--for..M9J"sden...S.ouares....lo.U.LaruLJJH3) See Table 8.4. 
. ...J - ...J 

<I 

<1= 

~ ---
>-' 

>-' 

o 

- _ ~ ~ ~ ~ M ~ ~ _ 10' .. '<T 

., , ," "''''~.r' ,tTI ,J'" , '""" , I , , '~.i)_ • '. , JUNE 1-30,1976 9 0.....-- \_ 

, , , , • "'.. - '~ •• FIG 9-D£VIATION OF SEA SURFACE TEMP!"f 

, , , ' , •• ..:- ", -' FROM 20'YEAR MEAN 11948·1967) 

. +', . . t ,. -+ .. ~ -. -i-. . + .. . - -+- '--:+".' ~ID.J(,() .:-:: SHADED AREAS COLDER IN 1975 ~ + , -~ ~ J - _ .. 4 ~F· I.I·e 

I I r-... ~ ~ • ." i- • _ •• ~ ---,: -.,... s-: '-~ . . ....., .., ~ ~ ~ u lf~ .' --

'-- -;- r- ~ ~ .. ~ .~~A ~ 111 

" 

11:1 

, , , • ~ -~ -. ~ -,~ f. • - r' . -. .. . ----=< ... " 

~ 

, ,' 

I ., , ~ , 

~ .... ~ ... --.-

•• 

-~:~ 

,.... .- - .. _.-. - ......... -- .~- '. ' 1., ........ _...... ' ..... ---!. ... ___ I -:-~ -.. ...... " ...... ~ ~ __ ~I/~ __ _ 

Poll - . -+- ... -.. --:,;,. ---- ." . . • + .. - m+ fJ - - - - -~ •. - ~ ·I~ • _ .• -. ,- I· - _w; '. . rn..: --t+ ~ ~ )-_ ....... ~f·.t jl.U ._ 

' - " - . ~f-+ " -:: ...:. :.:.:. = F: ~ , - "=-.. C:-. ~::: :-:--. ::. iJ ~ 

' ~ », t+ -r- I', • r-' ., --....- -,,--- ~ , 1 ' r;....--' .... ), - • - •• ~ • 

• I I ~ 1 l ~ I • ttl t I , I ~ I ~ 1 N ~~ -~ ; T -+--t ~ t- -+ 0- - ,... ---. iP' ~- - - • . . '1(- Wi ., 

-H-H+ l"~ f-;-+-+~ r T ~-z. ;..U . -+k ... , . ~~ ~ J 

L'l. 

L 

;:1;::,' 

L.l' 

;1.:, 

-12 

, _to_ .. _+ _+_+_. _ ... _ +_ + _ .. _ 

. T ' 

- , 

~H . .•. m-rt t I I' t +. ~: j.,:':" )(. ., .. ~ ~ ',-'TO. ., .. ,. - <9 .. .'- _ A -+-t A f-+-+~-" . _ ... t ••. I .. ~ _······t±ift·- _H_+;";~rl.J t\ •. ,- ~ <~. ·-· ~ .-..... L ~L .~ ~ fHH .....;. ,~ ,~~:.- r-... , , £~:f-"t-r ~ + : ~~~~ -. ~_ r~""' ~f'.t1-~ ~~~-:_~ !"'IT. I . O"A' . ~ ""'\ .. ~+~ T -i ~~"i+ :')=-:: f--. .- -

-+ 

I:,\-

...t~

" 

+-F f..~·H+ r=i++ ~$; - .::-~- - r~· ~. SOUTH 

-'--" "'-"' '-"' -"~-i' . ·tl ft .~.,- -. ' J- -' hj .. - -lot ) .. .,; H>r--t ~q ~~: L" -;( :-~ k'~~:~;' AKERlCA 

• I I I I I I I I I iT , F"'~'~"L .. 

' +- I t ~ / JI IA • :?P .-... "'- r--o----- ~/-V-'" ,W~ , ..l ,..r ., , . --+-+ +- :1i:..j:~1 . ~ 1 • •• • ~ •• -----. ~ 

W: +, "" . ~ - " ... ~-r'-t;;t;..t; ~~ -f-o-+-~. ++.- - ~J- • . ~ -...--......-- - - -;..","" i -!J ~ _ ____ ~ .... __ ... + ... f .... .. _~ +H+t+t++W-.-.-

- ... -. 

"- ............ 

, .. -... -,-.... -, r! 

f-'

....... . -'.0-+- .zj, ~E_ ./ 

7 j. - -t- +-•• -~ • " ., - - t .~ D,. •

+-+ "7"--+--'- - "', - ~ _____ ~ 

, 

+-+-.. -+-+- 6 - !... -.- . ' 

~ 

....... . I 

~ 

, "".t'. + •. 

" 

III' '~ : ' I : ' 'i' I : I I I . ...j...... I . I I', I I I I' ~ ~+., .:._+-.. ......... ---+----- , ' , ~ 

II H .-+-+.1 ~+T- ~ I : t-i--+-...... -+ u~ . .. . .' -........ , 18' II , I , , j! II ~t I I f- t,:; f-:- ++ i ·...,....... r+ r+........ '~ffi' I ~. +-. I . •

, • - ... j .... '1· _.L.... ~-+-............,..- .~-r.- ' .~. ; J 

: : : : t-r+-+ -t-'!- .+ t-+--J.-+-r I I: +-4- I .... l-l ~ 

II - - - -t-. --- -- ... ;- - - . - -. ---b- -r- .• - ';-i'H' -. '!1 tl-G1J.~t- .. + .;. '1'1- '1 -2T:t -~ T1T;';"i':' -:'~T:-:':-:-~' : -:-:-tr-::T:':- ·:.-r~~" -~ 

III I I , _I ' J 1 . +L Li..ll. [ -+' I i -r--r-"--+-l- ..... .l...!... • T.,. ~ .--oJ_ .~ + ~ • .t 

II 1 ' , '-t-I .. , , I " '.......,...-. .) '-- ~+.. -+-t+--+- ..... t" . ~. ~ . +-o----r-~ - ~ -t--+---+.......-r--- ''';;- , • , I I I I' , I I' 'I I I f! 

" I 

17 \ 

~ 

- , 1 1 -t+-jJ..L..-tt •• -'-+' -+f-'- • .J...! •• tt-o-........... ·- -.....I-.-.-.----~ .~~+-+-----------+-.________ ~ I " ' I 1 ·':11: . I 1 ' I ~' lI"'j m _ _ _ ro ~ 00 ~ ~ ~ ~ 

Figure 8.7.-Sea surface temperature anomalies (deviations, degrees F, from 1948-67 mean) for J une 1976 (from Fi8hing In form ation, 1976, No.6, NMFS. Southwest Fisheries Center , La Jolla, 

CA 920:18) 
Paper 9 

SEA SURFACE TEMPERATURE ANOMALIES 

Douglas R. McLain l 

~onthly mean £ea surface temperatures and their anomalies, or 

d epartures from a 20-yr (1948-67) mean, for 1976 have been mapped 

f or the Gulf of Alaska-Bering Sea, the eastern North Pacific, and 

t he western North Atlantic (Appendix 9.1). The western North 

Atlantic was mapped for 1974 (McLain 1976) and all three areas 

ere mapped for 1975 (McLain 1978). The maps are based on 

s urface marine weather observations made routinely by ships of 

many nations. 2 The observations are available in near real-time 

a nd at low co£t, and are used to produce several data products 

i ncluding these monthly mean maps. There are other maps of sea 

s urface temperature available, in particular g~lf~lr~~m 3 and 

i~hing InfQLm~liQn. 4 The areas covered are distinct and there 

a re a few important processing differences. Ei~~iQg IQfQrm~liQQ 

u ses the same 20-yr base period as the present maps. The 

t emperatures and anomalies are contvu r ed and thus reflect 

a nalysis; the data are not presented. The g~lf~lr~~m presents 

t he data and uses a full data set historical mean. The reference 

eriod includes years of sparse data, particularly before World 

I ar II, and clusters of data from classical research cruises. 

The observations of sea surface temperature were edited through a 

~o-stage filter. In the first stage, all observations <-2.0C or 

4DC were rejected. In the second stage, observations >8.0C from 

a reference value were rejected. The reference value was the 

base period mean for the particular month and the particular 

l Pacific Environmental Group, National Marine Fisheries Service, 

NOAA, Monterey, CA 9394Q. 

2The marine weather observations are transmitted worldwide over 

the GTS net~ork. They are received at the Fleet Numerical 

Weather Central, U.S. Navy, Monterey, CA 93940. 

3The g~lf~lr~~m' Oceanographic Services 8ranch, National Weather 

Service, NOAA, Silver Spring; MD 2091J. 

4Ei~hjD9 Inf9rm~liQQ' Southwest Fisheries Center, NMFS, NOAA, 

La Jolla, CA 22038. 

111 
Paper 9 

1-deg sQuare for the first two observations of that month; for 

Later observations the reference vaLue was the current mean for 

the particuLar mon th and 1-deg square. 

Saur (1963) and McLain (1976, 1978) discussed sources of error in 

the observations and in the maps. 

LITERATURE CITED 

McLAIN, D. R. 

1976. Monthly maps of sea surface temperature anomaLy in the 

northwest Atlantic Ocean and Gulf of Mexico 1974. In 

J. R. Goulet, Jr. (campiler), The environment of the United 

States living marine resources - 1974, p. 20-1--20.17. U.s. 

Dep. Commer., Natl. Ocean. Atmos. Admin., Natl. Mar. Fish. 

Serv., MAR~AP (Mar. Resour. Monit. Asses. Predict. Program) 

Contrib. 104. 

197~. Anomalies of coastal sea surface temperatures along the 

west coast of North America. In J. R. Goulet, Jr. and 

E. D. Haynes (editors), Ocean variability: Effects on U.S. 

marine fishery resources - 1975, p. 127-140. U.s. Dep. 

Commer., NOAA Tech Rep. NMfS Circ. 416. 

SAUR, J. F. T. 

1963. A study of the 

reported in logs of 

Meteorol. 2:417-425. 

quality of sea water temperatures 

ships' weather observations. J. Appl. 
APPENDIX 9.1 

The maps present by month and by 1-deg square the mean 

monthLy sea surface temperature, the d~parture from a 

20-yr (1948-67) mean, and the number of accepted 

observations. The temperatures ~ere not pLotted if there 

were two or fewer observations in that particular 1-deg 

square. ALso, anomaLies were not pLotted if there were 

fewer than five years represented in the 20-yr mean. 

AnomaLie& of magnitude greater than 1.0C are shaded. 

The rna ps cover the foLLowing regions: 

GuLf ::>1 ALaska 

and Be ring Sea 4SN-63N 122w-180W 

E as t er n No rt h Pacific 25N-SON 110W-150W 

western North AtLantic 20N-46N 60W- 99W 

113 
...... 

...... 

""" 

63 N I i I I I I I I I I I LrL<t"' I I I I I I I I I I ~~-r-r62N I' I" I I I I I I I I I II I ~~ I I I I I I I 1 1 I I I ++fIt-+-t 

61 N I I I I I I I I I I I I M~~;> ~-+-+-I--

NOAA - NATIONAL I1ARINE FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP MONTEREY. CIl.lFORNIA 

TEMPERATURE ANOMALY 

I- AT TI£ SER SURFACE IDEGREES CELSIUS) 

6e N I ' " , '" I "Vh IV( ~' .S .9 ., '--' - .- t 1 r"-'I IL 1 .jJV J r- '·1 J.,! ..,1 •• , 't'I)II"~' ¥ , " " i; ref JI , .; 3-1.8 ' ,~ fi . , ,,'I, 1 

59 NIl-' . !1 " l.J l- + ~ * .i -\\+-"\: + ~+ 

,.S ,., ,.S., t¢>~ \((~' I fl .r, "1",1 1.61- 1.3 J' -"' .S f'" I.l I t" '.2 I I.. ..., L .\. ~ \\ ,. l'l, \ It 

5B N I I I ' 2 " - ---- fl,.· - -;;. ' ~I' . 

,. " L' ." I 'l r ,. ,. ';; ~ '- ."It '.... -t;p~.7.. . +-.. -..;- l.9H f _~ U U J ' I, " I (\..~'\')'I 1\Ai·;..t, ' I 

< , I.l I.e Ii. - . '~ '. 

1976 J 1 .21 ·.1 1 I.' 

33U 

f-

""I 1 1 1 I I ':, : .. ,:, ., -;; .. - - ~--J ,,1: 4J t:t:;J f .. ,} <~"f"i+l 'i- I 

56N I I I ' ~...?. ,,~.-=-. - -'-/' /r-,yit t t fOal I TO .. ~ r t ~.a 1 t' .. \~&i~l~ ,i r .- +---t---I ~ ' . 2 •• k:' ~ ,:'5:1 V 2 " .:t 1 "j . "t . .. .. 4' 'I b' 1 J 1 If ~ ~ ~ .. ~ 7 I I 1 I -." !-:;,.5 +; 3 \ (I"J. \ 

55 N I '-- _ _ ,<. .. .. ~ ~ ~ ~ L ~ 0 ," , ~ ~ J II -, + + + + I I 

+.1 ".3".5 - .St .. J.1!I ~.3 .1 -.B2.ll - ·8 ,-. 6 ;-. 9 I 1 1.71 l -. 3 - .,+.0 - .0 . 2 1- .1 

54 N J 7 $ 1 <;I 1 , 8 ~ IS 6 13 ~ 11 I' I I I j , I ~ t <, ~ I • I .' l t "" . ~ t .. + t- t- t t \ ... t,l- + .. .. .. .---+ ~ 

"'1 ... 1 •. , 2.' J.I 2. ' J.' " •.• '.1 • 0' • " .-lr.J~ J.'" , ., " ,.... 1 '~"ll' •.•• • .• S"", 1"1 I 

7 

~ .• 

.. 

1.3 

.. 

41 

7 

3 . • 

2 

3. 4 

• 

1.S 

• 

l.~ 2 1. 11 

'S 

35 

.. 

J3 

,.('~ . ----;1 ,J 1\ 1 

j 

1,;5 

J'7 

+ 

., 

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_ j \'t

8 j _

;

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_

.8 _ ;1 I-LA. 

j 

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j _ 

.7 '",3 

' "_

.6 ;,

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9 ~1 l.e ;!l!_~~.0 j _'I!;I_ ;,2 .... 

~ ... 

~.e JI ,e; ;

'

9 

1 -+ 

8 9 

'I'" 

>, I 

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PACIFIC ENVIRONMENTAL GROUP HONTEREY. CALIFORNIR 

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JUNE 1976 NUM res 3972 

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t:~ r,P TEMPERATURE ANOMRL Y 61 N I I I I 1M. L= AT nE SER SURFACE (DEGREES CELSIUS) J--f--+--1 

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NOAA - NATIONAL MARINE FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP 

MONTEREY. CALIFORNIA 

TEMPERATURE ANOMALY 

AT THE SEA SURFACE (DEGREES CELSIUS) 1 

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NOAA - NATIONAL MARINE FISHERIES SEAVICE 

PACIFIC ENVIRONMENTAL GROUP 

MONTEREY. CALIFORNIA 

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PACIFIC ENVIRONMENTAL GROUP 

MONTEREY. CALIFORNIA 

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PUlA - NATIONAl IAIII£ FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP 

IOITEREY. Cfl.IFORNIA 

TEMPERATURE ANOMALY 

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I«Hl - tflTl(JjR PRH~ FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP 

POmREY. CIl.IFOONIR 

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PACIFIC ENVIRONMENTAL GROUP 

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lOlA - I*lTIONFt. IAIINE FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP 

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PACIFIC ENVIRONMENTAL GROUP 

~ POITEREY . CAll FORNI A 

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AT TIt: SER SURFACE (~GREES CELSIUS) 

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NOAA - NATIONAl MARINE FISHERIES SERVICE 

PRCIFIC ENVIRONMENTAL GROUP 

MONTEREY. CALIFORNIA 

TEMPERATURE ANOMALY 

AT THE SEA SURfACE (DEGREES CELSIUS) J~ 

JANUARY 1976 

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44 N I I I PRCIFI C ENVIRONMENTRL GROUP I( ~ /V r..vV V 1.6,~~2 ~'7 ~ .• 

MONTEREY. CALIFORNIA ~( 8/ 8 ,. 6 3 

43 N I 1 I TEMPERATURE ANOMALY 1\ IU 1) I L~~V ;rvv Iv~~~ / 1 /'2 / 'l ~'2 AT THE SEA SURFACE (DEGREES CELSlUS ) I ~ 114.2 '.2 4.4 5.. , .• . , 'ot 'l ~: ~~9 '1 :.5 :.6 n 

FEBRUARY 1976 Ie yf.-/V 1(; l -.3 -.3 +. 7 +.3 1( 6 -.6 -.9 0 -.3 

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45 N 

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43 N 

42 N 

41 N 

40 N 

39 N 

38 N 

37 N 

36 N 

35 N 

34 N 

33 N 

32N 

31 N 

30 N 

29N 

28 N 

27 N 

26 N 

25 N 

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23 N 

22 N 

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I Tl T T T TTl ~ ~ ~~ \. . II ~ ... 0-'/ - ·-1"l'=:"2 

I ,. 1\ " I \"2 V~P / 3 I 

N(Hl - NATIONfl. MARINE FISHERIES SERVICE I ( v ) ) ~p V v-'"'" V 2.2 ~ . ~ . Wk~ 

PACIFIC ENVIRONMENTAL GROUP ~ L.---;: r--v w'lJ· . 1* . . rrtt l 

I I I I I1ONTEREY, CAlIFORNIA U \ I) f....---"" ~ rr :.Hh2·j.ld',HIJ. I J. 261 

TEMPERATURE ANOMALY r\ ILf-' '- / / ~fl~I"i~" ,I . ;~~. -~I 

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AT THE SEA SURFACE (DEGREES CELSIUS) II .2,...J"l-- itrj'r :J ~r'·r!. ' .5 ij..ll .. t. ' .1 lfh 3.6 A.71' li'lt·~ '.2 I) I') I r I / !t"1'~ +.4 i1~1 +.7 1 .. ,. -.0 +.51'11 -.3 MARCH 1976 h I-f V lil ~ 1 211 1'J3j Ii 7 IT '5 ~"08S 5996 < ~V 1./ .~. )...3.~ 5.1 5.6 b]:J.r : ~l. 6.3 7.7:a~ I •.' - 4~+.3+.9 ~1~1r.~+.7-.11'+ +.6 ,-/ r-; 4 12 26 11 - trtf J U 1 J ~ '" 

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+.8 -.2 +.2 +.1 +.3 +.2 23 ZS 42 II 2 5 

I 23.2 25.5 U.2 ".3 ".5 23.5 

-.1 -.3 +.2 +.5 -.5 13 32 17 Iti I I I I II ~;'Sl m~~ffll ~;' l ~; 1 ~'9 

1

~ 

+. 2 

7 

m~~·91~'·81~·'I~·21~·S~~ • 5 • 7 • 1 • 8 • 8 I I ; . -~.-:7 ' ·'-"'5--:91--[-~mf~~I~'·71~'·S +. 6 ~ ~ .7.8 ~u~ .9 ,,wi ~ ~'.61~UI~UI~ .4 .7 .7 UI~' .3 .3 ·3 1 +.0 ".31~'·2 .5 - . 2 2 3 UJ 15 · _ " II _ 16 !I.?,,- ~ ,.I !',): .1,Sli 16 6 12 ~, J 7 7 .. 7 ":I R , 

I I A -Wlt lL~raJla\:roJ ~·~h.~·51 I ~ N :"81 ~'i Lf~ 1jJ ~1f:u I ~'51 ~'ll ~', I ~'2 ~~.1 h~!~1 :'6 1 ~'6 '.1 i 'I ~'l rr----r I v -rr'lt.t rm~'h1rnffbj'11 ~J I--r'\ I ~15 ~ iSl r . . :I ; 3 11 U1 Ii ~~ 1, 8 5 I I' ~ I' 9 

{ 1 

25.2 U.S 

~7 ~9 

- " 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 

II'> 
~N I I~AA-~TI~~~RI~FI~ffiI~Sffi~cr H~~~~'~~~~~~~~~~~~~~~~~ ~~~~~~~~~ ~~~~~~ 

.4.4 N I I I PACIFIC ENVIRONMENTAL GROUP . . - MONTEREY. CALIFORNIA ~-t---t.r7i\-+t-t---t--:;-:-t:;*~F-:-;;t--j~+-t~-t--t~-brt~r.:-+H+\-n-.h-h-I+t++'~~,-J-:,. 

TEMPERATURE ANOMALY 

.43 N I I I AT THE SER SURFACE (DEGREES CELSIUS) II d ..3rn:"~~'\ '3.6 7 ' .e •.• h.t ~.t :~. p ' .3 5.e ~ ... 6.5 

IJ r 1 ! -.3 -.9jt:l.jiJl.2 I' f ,1.6 -.4 +.9 . ,,-.111 

.42 N I APRIL 1976 J 2 - , 'I ,3 5 1 :'1': :,=>1 1\'7j 28 . '3 ] J ,2 

I NUll aBS 59SI!! ( 5.6 3.i ~~~ ~ ~:$ ~ 5.e 6.1 6.2 5.6 e. , 7.7 )~ 1 :)17,. ~.1 I""'---~ 1_ I ~~~ +.6 +.6 +.6 -.6 +.6 -.9 2.2~1.7S.2, 

.41 N • ~'-----,. ' .Y 9 " 39 12 " 15 16 : .. n,·! t ' ~~ 7 .• ~.~ 6.7 7.' 7.' )!;I!. 9~~ :!.s.,. 13.~ ,~.~ l~ i,M 16.' (l' ... B,l ~+.1 ,1.7+.3 +.6 +.3 I,!;! ~ f>~.~-.e ~.~ 2 +." 

.40 N I I I I I 1 1 1 1 1 1 1 1 1 1 1 I j I I j I I I. ~t 25 • I. ' e3 25 113 , If ,~, 17 ,~. jfil • 

I j I I ,) I t ',;~,' ~! ', ' I~ , :,Il'~ ', 'U :'7 .• '11.9 ,d., 118,' ~ '~ .9 ,e. ' 17.6 :Id. ~ r. 1-, 1.9 1 • .( 1.9 ~.7 :t.e ~.8 :t.6 !.5 z.e 3'.:4.~2.e +. 7 -.6~:t.l (! \..... :'Z8! ~ 'Nt ;~ 1 -' I~ ·:9.'· ' -I ~g 1" l?", pi" 'Q -i 8 8 , 

I 'I','-L 9.9 II.' 'H.~ 13.7 'ui., 'I,.' iI 8. ~ 1~1.9. ):19.;: "i,a " 1.2 ;!i'-~ 19.' 2I).a 

39 N 

" jt:l.!) +.5 +." 1~~ + ... !t-2~X 1~3jt;I!.~~2.-iIt:l~JiI'S'..4 2~0 1~0 -.11l ~7 

I I 1 1 1 1 1 1 1 1 1 1 1 1 I I I I I I I I 1_'<~('115": 2495'S' 115 ' 1'1 ' ' 7 "'2 ""Zl '9' 'i' 'Z" 3 '7" 38 N I~ \ . . ...., .. " ,. ". ' .. " ... " . 

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37 N I I I I I I I I I I 1 1 1 1 1 1 1 1 1 I' 1 1 1. r j 1 43 .. ; Ii!] 7 i J~ :~ '11, ;:4 1 :~: ~ I :7.1 5 

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36 N I I I I I I I 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 I :Ji 13 31 : I~ : • 'I~ II ~ 7 : ~ j "~: 3 3 

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35 N I I I I I I I I I I 1 1 1 1 1 1 1 1 1 Ill, tl~j hp1 13 3, II j~ 1 3 ' ;~ f:<' in ' 7 

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j +.3 -.9 +.4 +.6 +.7 +.6 -.5 +.6 1~1 +.5 +.2 -.2 -.1 +.9 +.8 +.7 +.6 III.I!! +.6 33 N ' I. 24 .'6 I. .. .j ~ .j 3 2 .7 ' 7 , 

19"lill1!1~' 23.9 24.5 23.6 ~~I ~ 21.' 21.B 2 •. 2 20.' 20.6 :~l~'f 2B .• 19.1 19.9 l~.~ , ~" . .t 28.7 19.1 18.6 19.2 

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I 21.3 24.1 25.. 22.6 22.6 22.5 21.3 21.2 21.6 21.'II~II~li" 28.' 19.e 2ll.3l!.J.7 21.2 28 ••. 1!I·t 

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31 N 5 IS" ... 13 7 rn" 5 1 : l~; 13 5 1~ 1 I 23.S 21.5 \ 22.5 25.7 2 •• 3 22.5 23.3 23.0 22.3 21.6 21. 1II 21. . 2'''9 ZS.t1 TI~' 29.1 21.. 21.8 n.? ~~.9 lJ.l 21.~ 2\11.7 

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29 N 1;V I ~ +.5 -.5 , \ 1~~ -. 1 +.7 -.1 +.11l I ~f' -.6 -.5 -.3 +.0 Ii ~ -.9 +." -.4 +.4 +.2 +.2 +.3 -.7 3 ~ 5 12 . 2 -hi3~. 1.4 11 9 5 !, I,: 9 A 6 Hi 13 : l; 16 12 6 -h~~.-' ~ 3 

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, '"II : • +.1 • .4.1 ~ +.2 +.2 +.1 ~~ .4 +.1 1.3 1.::\ .9 2A N I, I i, i·· t L 12 7 5 16 30 26 IIIMl" 23 l:9l'! fA it III . I~I!. 'ai' j. 3 7 9 12 6 5 3 ~ iSS 

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I I 25.7 ~~~ ~ '5.9 ~~' V ~ 1\ 25.5 25.3 25 21.7 25.3 24.6 24.8 24.7 l14;~ 25.6 ~~I ~ 25.' ,.., "l,~ UI~ I ".2 

22 N -.2 ;;2. -.6 :1' /::> I '- -.6 -. F-.5 -.7 -.7 -. 7 "'!~5 +.lld.~ -.0 -.6 1,2 I~ l -.7 -.3. II! I 19 ~ ! -'" Z 16 3 12. 1Z 15 Ild'i 6 .. .a ,.; Z 4 It Ie ZS.:f 2..-.-7 -;S.l 2i.6 ?5Jj 24 • .1 2.1.6 

21 N +',B -;9 -." -.9 +;5 -.9 -.5 

2

'" N r:~ ~~'9 ,t2 ]~~ t~ ~:'9 l11 v , ~~ "" ,11.. -.JI._.J..-',--,-,--,.wc. 

3 3 3 3 333 3 3 3 3 3 3 3 3 333 333 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 3 

m m ~ w ~ ~ m N ~ ~ m m ~ w ~ ~ m N ~ ~ m m ~ w ~ ~ m N ~ ~ m m ~ w ~ ~ m N ~ ~ 

m m m m m m m m m m m m m m m m m m m m ~ ~ ~ ~ ~ ~ ~ ~ ~ ~ w w w w w w w w w w 
.46 N , :;p="KJ"\<" i rt===5i 1· -r:::::. . I 

.45N I I I NOAA _ NATIONAL MARINE FISHERIES SERVICE I J'ifl 1;1 I I S0J - k I I J I T::l 7f '1 HLt:f··1 Hj 

.4.4 N I I I PACIFIC ENVIRONMENTAL GROUP 

MONTEREY. CALIFORNIA 

TEMPERATURE ANOMALY 

AT THE SEA SURFACE (DEGREES CELSIUS) .43 N I I I 

.42 N I I I MAY 

NUM OBS 5627 

1976 

.41 N I I I I I I I I I I r-T I I ~+-+--+ 

.40 N I I I I I I I I I I I I I 1 1 1 1 -+ -+ +- +-

39 N ! I I I I I I I I I I I I I I I I I -+ -+ i. -+-

38 N l it- +--t- + -+ 

37 N l it36N I~~~+-+-4-~~~~-+-+~~--r-r-~ 

35 N 

3.4 N 1 1 .1 + + -+ L + + .. 

33 N 1 1 'I +- + -+.. + 

32 N 1 1- +- -+ .j.. 

31N ~1 -+-+-4~~+-1-~-+-+~ 

30 N I I _ -' "'" I I '4 '9 I ....J-+ 

29 N 1 1 •.• 1 .1 < 1 f J .. 1 ~. r..:: 1 

28 N I ll fAlh~".1 '::,.1 ~.I " I ,',' .I .? .1 -:!r.:+ 

27 N 1 1 'N. 1 .# 1 ;1:, 1 .~ .I _ .. 1 _~ . 1 z'" 1 

26 N I .", UI },a.1 i' 'I • I ~.I ; .1 ,1,.-.+ 

25 N 1 I) Q 1 z 1 1 •. 1 ' 1 • 1 

2.4 N I It I 

23 N I I', I 

22 N I I \ I I -+ -I--+-' 

21NI 126.11 I I I I-I trt····t -'r~~~tll~~ 20 N 

:x 
~ ., \\ -_- ~': ~~.;r .r 45N " . NORA - NATIONRL MARINE FISHERIES SERVICE ( v ) ) "'-. -J /" 16.6 

U~ 8.' 

~ ~:~ ¥~ ~~. 

~1~3 8.5 

PACIFIC ENVIRONMENTAL GROUP V'-v +.4 ~ 1.5 +.3 

44 N Vr 7 2 :~I' :'?: :~~ MONTEREY. " CALIFORNIR U \ u L -ri ,,:3- ~ hr.? :~I.; .18.1 

~ }f1.1 / 11.8 8. lB .• lB. I 9 •• 6.' 

TEMPERATURE ANOMALY /" ~.? +.9 2'. 0 2~5 ~,~ +.7 +.4 -.1 ~.l 

43 N ~ "1l 'r ~ 5 ;it: : .... : ~ 1: ~ ~ 18. 27 3A 28 16 

AT THE SEA SURFACE (DEGREES CELSIUS) ) b~ -./ ---- X7 13.6 ''It "I.~ 

1~8 1~.3 11.3 "1.8 12.6 ,". ~ d.~ 

~/ ./ .7 +.6 1+:I.li I+I~l +.5 +.2 Ll +.8 ~Z 1.9 

42 N JUNE 1976 " , : r,..: I~ : :'1': 26 , :':1 II :~ : l 

NUM ass 5362 ( ../ "·11 .J6; :tl.7 ;U )I.~ :11., )l.~ '1U 15.3 \U 17 •• 1·1.4 

---- ~ ." ~.6 F.. ~ hi i+1~~ 1.1 3.1 +.3 1.6 +.1 4.1 

41 N ----~ , .3 , 1 1'(.1 : Lz." 18. la~ :3 : .. ~~ 1&.3 15.3 13.3 13.9 15.S .Ig.y 29.~ 16 ... <J.8 21.& IlI.s 19.B 

( • +.3 -.0 +.5 -.1 +.5 +.8 1+;3'~ i!.1 l.t/! ;3'~ ~.I' 1.3 ).5 

4~ N II I 228 8 12 62 28 13 ·8 ' ,it;.. 7. . ·9,· .~ ~ 

,/ 'I,.V ~'9.6 I~I) 16.0 '1~:2 18.0 '<:'1.7 tj . ., "3:6 t;:3.C cq 21.9 21.6 

($ '" 

:1.1 1+2'.0 ~"a -.1 2'. -.9 +.6 1+2'.9 I~ 1.3 1.8 -.5 -.9 

39 N 122: 13>' ,~ 8 't'3"' 9 I. " .' '9 . ,,,,. 

IJ< 1~.8 11.2 19.8 18.9 

-f~~ 21.2 21.9 2l!.B 21.6 23.6 U.l 2A.1 23.8 23.6 aU 

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38 N 1\ (' 23 249 ' 9 ~, 16 5 \I 1 a " 6 l 5 

21. 7 

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2 •. 16.S la.9 24.3 

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36 N 1.\11 : II 12 : w~ , 7 10 16 10 10 l '. ' .. , ~ 

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35 N 8 : ,II ~ \I I2T 3 6 13 Zl 17' 

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34 N 5 ill '3 8 Ie 15 2 5 3 10 10 '~ , 2 

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32 N 6 13 ' I. 7 235 6 , S ' S s ' , , 6 , 3 • . S , 

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31 N 13 ' 12 , " : 5 , 3 5 6 6 , :~ : 3 3 

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29 N 3 ~ !I ~ • " 10 ; z ; '3 16 :" . ~ , , • 

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27 N " ~' I I 2' 21 :13 I;, 6 , 3 ~ ' 3 2. I. I" 9 • 13 9 " • 7 '2 6 3 

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45 N I I I NOffi _ NATlONfl. MARINE FISHERIES SERVICE I ~'lJ I I ~ I I \\01 . 1,. r f- +---+ -J I +-L+ I I -t=1 :71''' '1 .. I::? r: .1 .. 1 

PACIFIC ENVIRONMENTAL GROUP 

44 N I I I IOITEREY. CA..IFORNIA 

TEMPERATURE ANOMALY 

AT Tt£ SEA SURfACE (DEGREES CELSIUS) 43 N I I I 

nl JULY 1976 42 N I I I 

NUll 085 54116 41NI I II I 1'1 1-1-+ I I I Il-t .. I I 1~~':'t1~~~.:.I;Llr'.rll';)J:::1YI.~.I;~~l 

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38 N I I I I I I I I I I I I + 

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36 N I I I I I I I I I I I I I II I I -t-I-.. t-. +-+ ~~ 

35NI I I I I I I I I I I I I +-+-+--+-f--+--+ 

34 N I I I I I I I I I I I I I -f--+-+ . + f-- + • 

33 N I I I I I I I I I I I I I+--f--.+ 

32 N I I I I I I I I I I I ~ -+---+-~+-+ 

31 N I I+~+-

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40 N 

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34 N ...... 

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32 N 

31 N 

30 N 

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f---+--+---il NOAA - NATIONAL P1ARINE FISHERIES SERVICE 4+---1--f-+-I--\~---'f.<:---+-t-+-t--+-~-+-t--'-t-+---+-+-:-:i:.::::::='+-;;;1"----=tmmmlh:::vrn:!Tt-::--:.l 

PAclFIC ENVIRONMENTAL GROUP 

I---+-t-II 110NTEREY. CALIFORNIR 

TEMPERATURE ANOMALY 

AT THE SER SURFACE (DEGREES CELSIUS) 

AUGUST 1976 

NUI1 DBS 5345 

38.5 

2 

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45 N I I 1N(Hl _ tflTlONFL ImIIE FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP 

44 N I I I tojTEREY. CIl.IFORNIA 

TEMPERATURE ANOMALY 43 N AT THE SER SURFACE (DEGREES CELSIUS) I I I 

SEPTEMBER 1976 ~Jr1 OOS 5.458 

j. j. 42 N I I I 

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32 N I I I I +- I I I + -+ + 

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44 N . I . - POCIFIC~Vr~N~NT~~OUPv MONTEREY. CAlIFORNIA I-

~~~M~~~~~~~~++4~~~~~~~~~~~~ffl~ 22.6 

43 N 1 1 I 

TEMPERATURE ANOMALY 1\ AT THE SEA SURFACE (DEGREES CELS1USJ rr I~ lI+t1 I I I I I II ~1~~ .jl~tU~5, L:l~~.1~~·5~);[,' ~k1t~~~~1~~·i fL-J I~; " 12 G~ ~E~ j G~ l 13 ITd'jiIll11nE!1'J" 3 

42 N 1 1 I 

611146 

OCTOBER 1976 

NUM OBS 

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45 N to¥l - '*lTIONFL Pf1RItE FISHERIES SERVICE 

PACIFIC ENVIRONMENTAL GROUP 

44 N f--+--+I-II IQjTEREY. CA...IFORNIA 

43 N TEMPERATURE ANOMALY 

AT n£ SEA SURFACE (~GAEES CELSIUS) 

42 N NOVEMBER 1976 

NJI1 OBS 

41 N 

40 N 

39 N 

38 N 

37 N 

36 N 

SN 

34 N 

33 N 

32 N 

31 N 

30 N 

29 N 

28 N 

27 N 

26 N 

25 N 

24 N 

23 N 

22 N 

21 N 

20 N 

:E :E 
r 45 N I I I I N~ ~ NA;ION~~ RINE FISHERIES SERVICE ;! cJ I . r+) ~""'r" ;:s . -/ . ~~-. -, -----:;~= / ~ ';'-IL~~~ ~1:k\~I; 

PACIFIC ENVIRONMENTAL GROUP I) ~ (\-vV"' 3) r')Fr~ 8r\~~ ~.m I I I I MONTEREY. CRLIFORNIA U \ U Z,.--<e i:3' •. ~ mI , 7.6 ~6.§. .r~:~,' ,I ,. , ., I/., !I ~II" 'i~, .44 N 

~ 

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43 N 

42 N 

41 N 

4~ N 

39 N 

38 N 

37 N 

36 N 

35 N 

34 N 

33N 

32 N 

31 N 

3~ N 

29 N 

28 N 

27 N 

26 N 

25 N 

UN 

23 N 

22 N 

21 N 

I ~ /':1f + SI""':.-t ;;;~~ 7 2 i2 ~~ . TEMPERATURE ANOMALY ~ -r-rr-Vz 1111 ; 5 Ili 1I1: ,~ ~ II I' I.~II. II I 

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Paper 10 

FLUCTUATIONS OF SEA SURFACE TE~PE RATURE A D 

D.E N SIT Y AT C 0 AS TAL S TAT ION S D URI G 1 9 76 

Douglas R. McLain ' 

Sea surface temperature (SST) and density measurements have been 

made routinely at many U.S. National Ocean Survey (NOS) tid 

gages and other coastal stations for many years. Although t e 

data suffer from various problems such as gaps in covera e or 

inadequate exposure to open ocean conditions, careful selection 

of stations allows the data to be used as an in ex~ensive monitor 

of climatic fluctuations in nearshore waters. This report 

summarizes monthly mean SST and density fluctuations for 197b and 

long-term means for three coasts of North America. The data are 

contoured in a common ~nner for each coast to flag unusual 

climatic events and to allow comparison of fluctuations betwe n 

coasts. 

This report is a refinement for 1976 of a s imil ar report y 

Goulet (1978). His plots were for 1974 an d 1975 only, as earlier 

data were not available in a computer compatible format. 

Subsequently, a computer tape of all avai lable historical ont ly 

mean temperature, density, and sea level data taken at NO id 

gage control stations was develope~. · The Tides Branch t 

provided update punch cards of monthly mean data. These data 

certain Canadian data ' were merged with the historical ap for 

preparation of this report. The data are now archived by e 

National Oceanographic Data Center and are available t roug 

their Data Services Divis;on. 

-

McLain (1978) presented time series of monthly mean anomali s of 

SST's at coa~tal stations along the ~est coast of orth A er;ca. 

Presented here are distance vs. time contours of lon -term eans 

and anomalies from the means for 1976 SST and density a selec d 

' Pacific Environmental Group, 'a tional arine Fis eries Servic , 

cIa Fleet Numerical ~eath er Central, ~onterey, CA 93940. 

OJ. R. Goulet, Jr. 2no E. D. Haynes:>1 he Resource Ass ss 

Division, NMFS, OAA , provideo for the edit in, e unchin, 2 

quality control of these data . 

L. F. Giov ando , Environ ent C~naca, Vancouver, B. C. 7 1 

Pers. corrmun. 

151 
stations along the coasts of North America (Appendix 10.1). 

The 1976 data are presented as anomalies from a long-term mean 

for the reriod 1948-75. This reference period differs from the 

1948-67 period used for other data sets such as maps of SST 

anomaly (McLain, Paper 9). The chan~e was necessary to develop 

means for certain stations which were established in the last 

decade. 

The stations used in this report are shown in Figure 1 0 .1. The 

stations chosen were those which had the best combination of 

dpsirable characteristics: exposure to open ocean conditions, 

long data records, minimum gaps in data records, and equidistance 

between stations. The ideal combination seldom existed and 

consequently many of the sat ions used were in estuaries, had gaps 

in coverage, or were at varying intervals along the coast. For 

example, data coverage is poor in Oregon and Washington as aLL 

stations are in estuaries or are subject to river runoff (as at 

Neah Bay near the mouth of the Strait of Juan de Fuca). Good 

coverage was available from British Columbia Lighthouses which 

have long complete data records from ~pen, exposed Locations. 

The data are plotted as contoured isopleths of the long-term mean 

and anomaly by month and station position aLong the coast. 

Temperature data are in degrees Celsius while density data are in 

sigma-t units [(density-1) x 1000]. Density values are computed 

for a s tan d a rd w ate r t em per a t u reo f 1 5 • 0 C • All m 0 nth L y mea n s 

represent at Least 12 daily observations. 

WEST COAST SEA SURFACE TEMPERATURES 

The Long-term monthly mean (1948-75) SSTls at stations along the 

west coast of North America (Fig. 10.2) had minimum vaLues in 

January and February and maximum values in July or August. 

Minimum winter temperature occurred at Kodiak, AK, while maximum 

summer temperature occurred at Los Angeles, CA. The winter 

minima occurred earlier (in January) at the southern stations 

(California to southern British Columbia) than at the northern 

stations, where minimum values occurred in February. Summer 

maxima occurred in August at aLL stations along the coast except 

at Neah Bay, WA, where the maximum occurred in July. 

Bakun et al. (1974) described the Long-term mean distribution of 

SST from ships in 1-deg squares of Longit ude and Latitude 

adjacent to the west coast of the United States. Their data show 

that offshore SST minima and maxima occur about one month later 

than at the shore stations. This may result from more rapid 

warming in spring and cooling in f~ll in shallower coastal 

waters. The summer maximum temperatures reported by Bakun 

152 
et al. (1974) are similar to those at the coastal stations but 

winter minimum temperatures are about 1C lower at the coastal 

stations. This depression of coastal coastal temperatures may 

result from the lower heat capacity of the shallower water column 

at the coastal stations as compared to the offshore areas. 

Both Figure 1C.2 and the figure of Bakun et al. (1974) show a 

horizontal trend to the isotherms near Point Conception, CA, 

oetween Port San Luis and Los Angeles. This "flattening" of the 

isotherms is an indication of change of ocean water masses at 

Point Concept jon between the cold California Current water to the 

north and the warmer water of the Los Angeles Bight to the south. 

Dur;~g 1976 the anomalies of SST's at coastal stations were 

rather noisy and the only major trend ~as t~e presence of cooler 

than normal water along the CO?st during spring and summer from 

Sitka, AK, south to California. During summer, first in 

southeastern Alaska and later farther south, the anomalously cool 

water was replaced by warmer than normal water which reached 

maximum anomaLies of +2.SC at Yakutat, AK, and off southern 

California in November and December. 

The SST charts presented monthly in Ei~hing In!Qrm~tiQQ showed 

general negative anomalies of SST along the coast during 1976 

until July when positive anomalies first impinged against the 

Oregon and southern California C0asts. Positive anomalies spread 

during summer and fall and occurred along t he entire coast in 

November and December, in agreement wi th the coastal station 

data. 

WEST COAST DENSITIES 

The long-term mean di~tribution of density along the west coast 

of North America (Fig. 10.3) showed that minimum densities 

occurred off California in February, probably in response to 

winter rains. In Alaska, however, minimum densities occurred in 

June or July due to snow and ~l3cial ~elt. 

Durin~ 1976, observations of density were spotty but showed 

positive anomalies off most of the coast most of the year. Large 

positive anomalies of density off San Francisco and Crescent City 

were associated with drought conoitions existing over California 

most of the year. The low densities at Kodiak, AK, in August and 

September were apparently in response to Local precipitation. 

153 
,

EAST COAST SEA SURFACE T~MPERATURES 

The long-term mean SST's at stations along the east coast 

(Fio. 10.4) showed minimum temperatures at all stations 

Jan~ary-~arch, and maximum te~peratures July-September. As for 

the west coast, the peaks were earlier (January and July-August) 

at the southern stations and later (February-March and 

Auaust-September) at the northern stations. Minimum winter te~peratures of 0.6C occurred in February at Portland, ME, and 

maximum summer temperatures of 30.7C occurred in August at 

Key West, FL. 

Two regions of rapid change of SST with distance can be seen 

(Fig. 10.4). These regions are between Kiptopeke Beach, VA, and 

Myrtle Beach, SC, and between Mayport and Miami Beach , FL. As at 

Point Conce~tion on the west coast, these regions are associated 

with changes in ocean circulation and occur at Cape Hatteras and 

Cape Canaveral, respectively. Unlike Point Conception, however, 

where the greatest SST change between adjacent stations occurred 

in summer (4.0C change in August), the greatest changes in SST 

between stations on the east coast occurred in winter or spring 

( 8 . 2C change in January at Ca~e Canaveral and S.7C in April at 

Cape Hatteras). 

Durinq 1976, sampling at the stations ~as incomplete and many 

values were missing . In January anomalies of SST were negative 

along the entire coast as were air te~peratures over most of the 

eastern United States (Wagner 1976). Anomalous ~arming occurred 

in February, and by March SST's were above normal along the coast 

(up to 2.6C above normal at Charleston, SC). This warming also 

was mentioned by Taubensee (19760). During the summ~r months 

anomalies were positive at Montauk Point, NY, and to the north 

but were negative to the south. SST's were generally below 

normal during the fall, and became extremely cold in November as 

the unusually cold winter of 1976-77 began. An extreme negative 

anomaly of -S.SC was observed at Sandy Hook, NJ, in November. 

Chamberlin ana Armstrong (Paper S) summariz ed air temperature 

data along the east coast tJ show the developm ent of the winter 

of 1976-77 when strong northerly winds occurred over much of the 

eastern United States. Their data, from National Weather Service 

weather stations for the perioD July 1976-J anuary 1977, indicated 

t hat an 0 mal i e.s 0 f air tern per a t u res i n f all 1 9 76 w ere m 0 s t 

negative during November over most of the coast. This is in 

agreement with the SST data. In neither the air temperature nor 

the SST data did large negative anomalies occur as far south as 

Miami or Key West, FL. Dickson (1977) also showed that southern 

Florida air temperatures were not unusually cold in November. 

The strong negative anomalies of SST in November were a response 

to the extremely southern location of the jet stream and the 

consequent cold, dry winds from the north and northwest. These 

154 
atmospheric ~onditions enhanced heat loss from the water, 

strengthened southward-flowing coastal currents, and increased 

vertical mixing. Evidently these processes were not fully 

effective at Miami and Key west where SST's are more closely 

associated with Gulf Stream advective processes. 

EAST COAST DENSITIES 

The long-term mean density data on the east coast (Fig. 10.5) 

show that many of the stations are affected by land runoff. Such 

runoff is particularly evident in the figure at Boston, ~A, 

Sandy Hook, NJ, Kiptopeake Seach, VA, and Charleston, SC, where 

closed contours enclose regions of minimum water density. 

Minimum den£ity water occurred at the northern stations 

March-May, while at the s~uthern stations it occurred 

January-Apri l. This delay in the time of minimum density at the 

northern stations resulted from retarded snowmelt and river 

discharge in spring in the north relative to winter precipitation 

in the south. The timing of maximum water density similarly is 

delayed to the north as maximum density generally occurred 

May-September at the southern stations and during September or 

Octaber at the northern stations. 

During 1976 density observations were frequently missing, and the 

available observations did not have much cohe rence from station 

to station or month to month. A re g ion o f coherent positive 

anomalies occurred from Montauk Point, NY, and north over most of 

the year, with the obvious exception of Boston, MA, and Portland, 

ME, during January-March. positive density anomalies at 

Woods Hole, M.A, and Montauk Point increased rather steadily 

during the year. 

Large and variable anomalies occurred at Charleston, SC, and 

Mayport, FL, and resulted from fluctuations of river discharge 

near these stations. For example, the positive anomalies of 

density at these stations February-May were associated with 

drought during February and March (Dickson 1976a; Taubensee 

1976a). Similarly the negative density anomalies at these 

stations in June were associated with higher than normal 

precipitation in the area (Dickson 1976b; Taubensee 1976b). 

GULf OF MEXICO COAST SEA SURFACE TEMPERATURES 

The long-term means of SST's at all stations along the U.S. coast 

of the Gulf of Mexico (Fig. 10.6) showed minimum values in 

January and maximum values in July or August. Minimum winter 

temperatures occurred at the most northern, estuarine station, 

155 
Dauphin Island, AL, and maximum summer temperatures occurred at 

the most southern, open ocean station, Key West, FL. 

During 1976, observations of SST's at Gulf coast stations were 

fairly complete and showed good coherence in space and time. A 

pattern of SST anomalies similar to that observed at east coast 

stations fram New Jersey to Florida occurred. SST's were 

anomalously cold at all Gulf coast stations during December 1975 

and January 1976 with the greatest anomalies in Florida. 

Anomalous warming began in February in Texas, and SST anomalies 

peaked in March at Cedar Key~ FL. Anomalous cooling then 

occurred over most of the area for the remainder of the year, 

peaking in the large negative anomalies of Novemb er over most of 

the coast. The negative anomalies in November were <1C in 

magnitude only at Key West, FL. The greatest negative anomaly 

(-S.1C) was at Galveston, TX, in November. Chamberlin and 

Armstrong (Paper 11) in their summary of Gulf coast air 

temperature s during late 1976 also found greatest negative 

anomalies at Galveston during November. The anomalies of air 

temperature were caused by strong northerly winds, whereas the 

SST anomalies were caused by heat losses to the cold, dry air. 

GULF OF MEXICO COAST DENSITIES 

Long-term mean water density (Fig. 10.7) ranged from almost fresh 

in January at Dauphin Island, AL (in Mobile Bay), to open ocean 

conditions at Key West, FL. The months of minimum and maximum 

densities varied and reflected variations in timing of local 

river discharge. Minimum densities occurred January-June and 

maximum densities occurred June-November. 

Anomalies of density in 1976 ~ere variable, and apparently were 

related to local fluctuations of precipitation and runoff. 

Negative anomalies of density were observed almost all year at 

south Texas stations. Positive anomalie s occurred during 

August-October from Dauphin Island to Key West, and into December 

at stations io southern Florida. 

SUMMARY 

Although coastal station data are noisy and have frequent gaps in 

coverage, they do show large-scale coherences among stations. 

These coherences are in general caused by climatic fluctuations 

that affect long stretches of coastline. An extreme example of 

such a climatic change is the strong northerly winds over much of 

the eastern United States during November 1976. These winds 

created negative anomalies of SST at coastal stations of at least 

156 
Paper 10 

·1C in magnitude from Portland ME, to Mayport, FL, and from 

t. Petersburg, FL, to Padre Island, TX. Extreme anomalies of 

,S.SC were observed at Sandy Hook, NJ, and -S.1C at Galveston, 

'x, in November. 

LITERATURE CITED 

AKUN, A., D. R. McLAIN, and F. V. MAYO. 

1974. The mean annual cycle of coastal upwelling off western 

North America as observed from surface measurements. Fish 

Bull., u.s. 72:843-844. 

)ICKSON, R. R. 

1976a. Weather and circulation of February 1976. Extreme 

warmth over the eastern two-thirds of the United States. 

Mo. Weather Rev. 104:66 0-665. 

1~76b. Weather and circulation of May 1976. Temperature 

reversal over the United States. Mo. ~eather Rev. 104: 

10~4-1089. 

1977. Weather and circulati on of November 1976. Record cold 

over so~th and midwest for the second consecutive month. 

Mo. Weather Rev. 105:239-244. 

GOU LET, J. R., Jr. 

1976. Tidal station temperatures, u.s . east coast and Long 

Island Sound. 10 The environment of the United States 

Living marine resources - 1974, p. 19-1--19-9. u.S. Dep. 

Commer., Natl. Oceanic Atmos. Admin., ~atl. Mar. Fish. 

Serv., MARMAP (Mar. Resour. Monit. Assess. Predict. Program) 

Contrib. 104. 

GOULET, J. R.I Jr. and E. D. iAYNES. 

197b. Coastal temperatures. 10 J. R. Goulet, Jr. and 

E. D. Haynes (editors), Ocean variability: Effects on u.s. 

marine fishery resources - 1975, p. 21-23, 34-39. u.S. Dep. 

Commer., NOAA Tech. Rep. NMFS Circ. 416. 

~1 c L A IN, D. R. 

• 

1978. Anomalies of coastal sea surface temperatures along the 

west coast of North America. Io J. R. Goulet, Jr. and 

f. D. Haynes (editors), Ocean variability: Effects on U.S. 

marine fishery resources - 1975, p. 127-140. U.S. Dep. 

Commer., NOAA Tech. Rep. NMFS Circ. 416 • 
Paper 10 

TAU8EN tE, R. E. 

197ba. We~ther and clrcul t;on of h v y 

precipitation around th r t r 

1J4:t.09- 14. 

197 b. we",ther and Clrc l t10 of Jun 1 7. Inc r 

droug t in C l,forni o. a h r P . 1 4:1200-1205 . 

~~GNEF<, A. J. 

1976. ~eather and circulatio of J 1 76. Incr 

drou~ht in Calif rnl nd th so r Pl I n . o . heather eVe 104:41- b. 
10.-

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.. 

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DAUPHIN IS , A L 

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.a ZI.9 211. IS.2 18.9 19.3 IS.5 ~.2 21.1 21.S SITKR. RK II.-i -. 9 -.q "0;1: -. 

23.8 23.9 .8 23.7 23.8 23.8 23.7 23.7 23.7 LRNGRRR [S. BC -.1 11.3 11.3 B.1 S.l 

.8 .8 • 8 23.8 23.7 Z3. 7 23.7 Z3. S 23. B 23.8 CRPE ST JRMES. BC 

.6 .J n.s 23.6 23.2 22.2 11.6 21. 2 KR[IIS [5. BC 11.3 -.2 -.3 -.11 -.3 

21. I 1.6 22. .6 .7 72.7 22 •• 21.6 21.1 .B RMPH[TR[TE PT. BC -.3 -I. B -. 1 -.7 -.. 72. 23. J n.6 23.7 23.7 23.3 22.7 22. i IIEAH BRY. :IA - .6 -.8 11.3 ~ I •• 

I. I. .5 lc" •• 3 2'.3 ~1 22.B Ih.7 CRESCENT CITY. CA 

.6 1.11 1,1i .3 .9 .7 23.6 23.1 22.. SA .. FRANC:'5CO. CR 3.5 ~, ••• '.3 

4. •• • • •• .. .2 2501 "'.9 ( • • 9 POII' SAN LUIS. CA 1.2 1.6 I.. r:5 

.It .2 .1 .1 4. ' .B LOS LES. CR B. ) 11,1 1.5 B •• 

' .. .It .2 .. . 8 4 . A.8 .1 .1 II'J'ER 1 RL BCH. CR '.2 1.2 1.1 

8~197S DE:NSHY ONTHLY A~DMRLIES 

[0 r 1945·75 (len) lind anomallr-I (or 1976 (riJ;hl) o( drl18it) (,Igmn ·1) alon!: lh,! l. .~. 

I.B B.7 2.5 '-, I.. I. I I. I 1.8 1.8 

-:7 \1.1 

11.2 B. 1 

-.5 -1.11 

).'.. -.3 

" 

" 

B.l 

\ '.,. 

.1 

B.I • ••• -~ . 

-.7 -.3 

-.7 -.9 

11.6 B.2 ~ _ :.2 -.1 

3.7 3.3 2.7 2.6 

1.3 1.1 1.1 .6 

1.1i 1.7 •• 5 1.1i 

DENSITY 

t ,:oa.l. C-oniou r Inlervol 

".;---- - - B.' -I.. -1.2 -.8 

~I It. 1 . a 1.3 

-. ' \ 1;8 I .• ,,-.. -,7 ~~ l I •• I •• 

'.2 '.5 1.& 1.3 

2:1 3 •• 

'" l.a 2. 1.1 1·2 

.7 • 7 1.4 1.5 

I. '.$ 

unll 
... 

2 

D J f 

r 

~7 

~ .. , 

i

& 

2. 

,7 

" 

l1\~'4 2:9 ~5 3.1 · 6,· 

I 

~ 

""" 

N 

2217- Q!. t <2. (- 23. 5. 

22\.a--~.1 24\ a 

A 

TERM MERN 1948- 1975 

N J J A 

!ha- 1&,1 

23.3 

25.2 

27..&-- -21.6 

.7 \.6 26.~ 

27.9 ..Je.1 ~ 

30.5 

30. 7 

SER TEMP 

5 

27.5 

,.6 

17 

\ 21( Ira 

\2211 ~. 

\ \ 

24\1 19,5 

7. 2 )24.7 

2V.6 U. 

1976 

D D J f N A N J J A 5 o N D 

6.3 EASTPORT. ME B~~~~~ , ~ 12 la 

~ 8 PORTLAND. ME 

~'3 -:J' c· ~ ~6 ~ -¥ ~l.B -hi- ([\ 1tr1- • -=-.7 

6.7 

la.9 

\ 

\ li"0 

15.6 

ft. 7 

22.3 

BOSTON. MA 

1010005 HOLE. HA 

1:7 B.5 -<f::- 1.4 1.1 ~ &'·5 &''' 

;: " I. \ -.7 ) B.5/ 1.5 B.6 B.4 B,7 

Q~ I ~ 

rI ~z ( -'r (5 -2.5 

\ 

NEWPORT. RI 211 

MONTAUK PT. NY 

SANDY HOOK. NJ 

ATLANTIC CITY. NJ 

CAPE MAY. NJ -.3 

KIPTOPEAKE BCH. VA B.9 

MYRTLE BEACH. SC 

CHARLESTON. SC 

MAYPORT. FL 0.7 

MIAMI BEACH. FL -.2 

KEY WEST. FL -.2 

{.2 

~ ):r. 1. 3 

-1. 9 ~.5 ) 1.3 

B.6 2.5 

-.? \ t.4 

\ \ "-

-UI \ 9:,9 ' 2.6 

\ \ \ , \. ".2 \ 1.7 

\ \ -.8 -;~ lfB 

-z~\.61 A 

MONTHLY RNOMRLIES 

+-- t 

~ -.l "-J,B ;.~ -2.B 

~~.s- ---- ~/t'4 -...../ 

/-:~ tJ -)::'-=~:4~b7 -~' ~ ~'i -·1 -f' 

,9 J I 

-.7 .0 -.11 

1: \ -.,' -., .4 -2.B 

'-. 4 -.. f ~.3 -.1 -:-9 

-1.4 

'-...-

BA:.. -:B,.i 

-I.B 

-. 4 -.4 

SER TEMP 

-.6 I -1.6 

-.3 

I 

-~ 6 

-1.5 

~ -.-1- e 

Figure 1O.4- Long-term mean for 1948-75 (left) and anoma lies for 1976 (right) of sea surface temperature (degrees C) a long the U.S. east coast. Contour inteT\'als are 2.0C fo r mean and l.OC for 

a noma lies. 
o J F M A M J J A 5 o N o 

23.8 231

4 23[6 23[9 --2 ... ,\ 24r2 24 :3~ 23.B 

---+----r--

21~ ~3 ~.B 

~~ 

!B~.2 19 21.3 

-- 211 4 28~a 21.8 21.8 21.2 211.5 2e.' 

23i6 23.4 23[ 3 23[3 23[3 23[ 4 23~6 23,6 23.6 23.7 23.7 23.6 23.5 

22r7 2216 22r 2218 5 22i3 22·,B 23.8 23.2 23.3 23.5 23.4 23o! 22.9 

22,8 22.7 22.6 22 5 --2·}. !j b!.1 22.4 22.6 22.S 23~.3 ~9 

17; 2 17r 16,7 16~.1 ~ l~ IB.7 ------ ISo! IS.2 IS.I 16.4<::11: 2 

23.11- 23.e 23r" : -a.s 

==---------

23.e 23." ------ 23.3 23,4 23.3 23.3 ----- 23.2 23-:2-a" 

211;5 3 211.7 2II:s---n. 7 21.6 21.B 211S 21-.g--2J.3 211.7 2e,5 

I 

19.:l _~ 19.2 1819 18.4 ~ IBf5 IB B . e 2C:::.3 

25.' 25.~' 

T ---------' 

TERM MEAN 1948-1975 DENSITY 

1976 

ERSTPORT. ME 

PORTLRNO. ME 

BOSTON. MR 

I.JQODS HOLE. MR 

D J F M A M J J A 5 0 N 0 

.~. ~ .,. r 1 'r' GI I -',' -" -"~.,, .,' ,,~ /." - '[' I,a 

\ I I -.3 - .9 Y I.rz.a--z...t----J I.S -h7 1.2 1.a '-------- ,,~ 

1,1 I." 9.9 1,3 1,3 1.5 1,6 1,6 1:8 I

r

9 2ta~1 2,2 

NE].JPORT. RI -~ <::iX 

MONTRUK PT. NY B.7 B.6 9.6 B.B La -------------------------------- 1.5 1.5 1.6 1,6 1,5 1.5 1.2 

SRNDY HOOK. NJ 

RTLRNTIC CITY. NJ 

9 .... ~ , '-...----------

e.B e,5 8.B 9,5 e.6 

-2~,.--:2,7 , -Le) e,B 

-.4 e,3 

." 

CRPE MRY. NJ -.5 -1.7 -1.3 -.6 

KIPTOPERKE BCH. VR -2~ ~ 

:L~.' .,' lB. -.5 -.' e , I (' -.' 

"" r;s"f" 

-1,3) -2:5 flt6 

MYRTLE BERCH. SC 

CHARLESTON . SC 

MRYPORT. FL 

MIRMI BERCH. FL 

KEY ].JEST. FL 

.-/ 8r- . 

3,6 

ro 'Yr ;: 3.~ 

....... --....,. -1,5 \.6 

-2\ L 

8t 7 e.7 e.8 

ei6 e.5 e.5 

MONTHLY ANOMALIES 

1.2 1.1 1,9 t-

'::(t -V e,2 

~ 'r-4 8.7 et 4 r 

~a 

~4 

Bt-l-- 8r8 Ul 

DENSITY 

Figure 10.5.--Long-term mean for 1948-75 (left) and anomalies for 1976 (right) of density (sigma- t) along the U.S. east coast. Contour interval is 2 units. 
1976 

OJ F M R M J J R SON 0 0 J F M R M J J R SON 0 

17.5 14.9 IS,! II Zl.); / 4.7 26.4 26.1 26.6 26.~ 2S.9/2:,6 l'S SOUTH PADRE IS. TX -.1 \' \2 2.B y9 -.2 B.6 B.2 B.2 Bf \ -.~8 \"3.4 

16( . ..., ,~ \..( I".{ ,l r~2 29.2 26.' /..'" l/ ",' "" "''',,>D. "'\' -" '-\" «.<' (:\-J:'\\~/ 7' r.2- \ \ B)1 2'r -4,6 -:~5 ,-...., \\\\\ \ \ ~\rJJ 1,1 \\ '; \ 

16(..5 ~'6 ' 17.\ ~B \ 25.\ ~.4 29.4 29.6 26) f /1 / .,6 i 161" PORT ARANSAS. TX -.1 -., / i

ll

.

s 

'\ '\ \ \ /, / / /" \ \ \ I. J ' I. I FREEPOR' TX I 14t

B 12J3 13. .7 \ I'r / 2S.2} 27. 28.6 29.3 2?E 2I

j

"/ 1,9.) j14.6 , . -.1 B.4 1 2.7 

I I I I J ,I '\ 

U. 12.4 13.), " \ ,.\ ~'\ L ",' .... J, ":': j.,.' / .. ,' "",,,,,, "", "-.. -," ,., ... !"'! f .. , -,.r 2-.1 -,4 -, -. ~l -t.B 

" \ \\ / ,I"'l /\ I II 

13.4 10 )2.4 16 B .4 ) 21. 1 2B,' " 29,1 29." ,'27,'" 7~.:t flrl; 13.4 DAUPHIN IS. AL -.3 ' -I.~ I /2[ 9 ~,7 (, B. ~ \-I .B -1,7 -.7 -.B -.) \ 2, -3.6 1-2.6 

~ \ I \ I 11 

\ \ 1 I \ \ I I \ ,. • 

14~!\ 13.1 ) . -:4 1.6 25,8 26.7 29.6 ,z9.9 27: D ,~.S\ '\16,1 14.3 PENSRCOLA. FL .2, -1.1 "I.~ 2.4 ,I.~ \ -),4 ;-.6 " B.3 ' -.3 -.1- -3.5 \ 2.S 

". / ( \ \" \ ' I, ' '\ ,\ (r-'\ ,/ t \ 1\ \' \ ' ",\ ' A I 

IS.4 14.7 IS .1 iE.9 29.3 '.1 3B.I 2B.~ .?.'.\, \ 13. 1 lS.1 CEDAR KEY. FL ~ "z.;: B.B 3.3 B.7 , t.\ I {I.S- \~~ •• , -3.E .2.7 ( \ • I I " I ~ , 1 

17~.9 1],.5 S' 3.~ j.4 26.S 29.1 29.7 2e.~ , 25.4' Z) . I 17,S ST PETERSBURG. FL -.1\ ~2. ' • . ~ 1.9 B.2 -.~ -I.B \ B.6 B.4 '\1 \I) ~ ~ ;:6 ___ . __ / \ I I \ , I \ \ ,"--- ............. 

22~ 21.7 n<r/ 24 .. " 2S.7 27.§ 29.7 3l!.4 3B.7 29.7 27.6 24.S 22.3 KEY \JeST. FL - .2 -Z.2 ".6 1.2 ~.3 -.1 - .9 - .4 -:i, B.S " -.2 -:':r -~~ .B 

TERM MEAN 1948-1975 SEA TEMP MONTHLY ANOMALIES SEA TEMP 

Figure IO.6.-Long-term mean for 1948-75 (left) and anomalies for 1976 (right) of sea surface temperature (degrees C) along the U.s. Gulf coast. Contour intervals are 2.0C for mean and I.OC for 

anomalies. 
o 

ZA. l 

ZS.fI 

ZI. 

18. 

19 •• 

.8 

J 

lJ.li 

l,4 

11.2 

.8 

F 

".2 

.B 

1'2.l 

17.7 

Si. 

k'.II 

19. ( 

M 

U.6 

23.3 

ZZ.J 

17,4 

7.1 

tlhll 

Ifh-. 

R M 

".72l.7 

ZA.4 .-- 23.3 

nc<9 28.7 

uw; ..... 15.' 

7.1' )8., 

8.' -11,3-

17 .s. ~ rs71 

J J 

2Ij.4 V.I 

1~ .• 3 \ 22.' 

\ 

16.S IS.6 

11./i ll.6 

j 

13.5 - U. t 

21" 2 2I!.B 

R 5 o N 

V.3 26.~ 24.S ZS.B 

{s /7.6 ' 'k.4 (j ./ /;...- 26.8 ~ --zr:3 28-:-S 

--- 2 •• -2 Ir 1~"8.2 

2},9 .uL6 lB,S IS.B 

T2:6 I3lIh 14.3 15.2 

13.3 ~ 15.4 - 10:' 17~8 

19. I IB.6 19.' .2(.3 

o 

24.4 

25.B 

7hS 

18.3 

19.1 

I~' 3 

1-5.8 

~B 

1976 

o J o TX F M R -2.5 , _., IB M J J 

\ 

. B.7/' -.7 _ R 5 0 

) 

~.8 -.2 -7 N 

TX . • -.3~ --5.3 .5<;' _ G ~ - ~ .7 

PORT RRRNSRS. TX -2 .6/~ 1 -.7 ''-. • .----;-;- J 1 ____ 1. \ ' ~\3 l·rlfV;; '--- I" . ~ '\ ..g.B 

. ~ ~\2 -. k,O- . "-- ' 

FREEPORT. TX _ " . -.6 '\.,.-2.7 

SOUTH PRORE IS. 

PORT MRNSFIELO. 

-".4 ",,-

"4t.2 

GRL VESTON PRZI. 

ORUPHIN IS. RL 

PENSRCOLR. FL 

CEORR KEY. FL 

B.5 1.71 /. .( ~ 1.1 -i.\2 A I ,,--) .8 BJ ;-3.3 

:l'.8 j. I / '\ . ' .3 B 

1.7 ~ -~------ ----=2. --- ~ '" ~ ' ,--...- '-- -" '71J~3 \ ) -3.5 -3.:9 -5.~ -J.-3.-~· _ 1/ r ) /''-- 1 (S ( (-Elf!' . 

TX -. S\ 

-J. 6 \ 

-1.1 ---- -J. 2 .~ \ 4<! 

2.B 3~ h '\1\\ -\,4 

\ "-

-.6 '-1'.4 

"---

B.8 II.S 

,..--

. , -r; 3 

-: 3 

19.' 19.3 IS.S / 28.6 21.3 28.7 .lB.9 l U_A- 11.i.o IB.9 19.' ST PETERSBURG. FL -2:S -.9 \l.S 

\ 

1.2 B.B ) -.7 

27.1 V.3 V.6 27.2 V.3 n:z 26.S- 2It.r Z7:1J 26.9 KEY \.JEST. FL -2. ~I 11.6 II.S B.S <a -.• -.1 ~ 11.2 B. 

TERM MEAN 1948- 1975 DENSITY MONTHLY ANOMALIES DENSI TY 

FiICUrl' I () .7. · I,onj(·t,·rm mpun for 191R-7:; (left) and anomalies for 1976 (right) of density (sigma-t) along the U.S. Gulf coast. Contour interval is 2 units. 
APPENDIX 10.1 

L oc at ion s 0 f s tat ion 5 s how n i n F i u r 1 C • 1 • 

~~§ 1. £Q.~§1 

Adalu AK 

Unalaska, AK 

Kodiak, AK 

Ya kLJ tat, A 

Sitka, A 

Langara Island, B.C. 

C~pe St. James, B.C. 

Kai~s Island, B.C. 

Amphitrite Point, B.C. 

N ah Bay, WA 

Crescent City, CA 

San Francisco, CA 

Port San L is, CA 

Los Ang~les, CA 

Imperial Beach, CA 

s~~l £Q~§..t 

§!J.!.i 

E a s tp 0 r t , E 

Portland, ME 

Boston, MA 

Wood s H 0 l e, ,..., A 

N e wp 0 r t, R I 

~ontauk, IY 

Sand y H 00 k , J 

Atlantic City, J 

C are May, NJ 

Ki pto~eke Beach, VA 

rtiyrtle Beach, SC 

Charleston, SC 

M a yp 0 r t, F L 

M i am i Be a c h, F L 

!(ey west, FL 

Q1 ~~~i£Q £Qg§! 

Padr e Island, TX 

Po rt Mansfield, 

Po rt Aransas, TX 

Freeport, TX 

Ga lveston, TX 

D a uph in IsLand, 

Pensacola, FL 

Ceda r Ke y, FL 

St. Petersburg, 

Key ~'est, FL 

TX 

AL 

FL 

166 

57 '0 ' 

54 5 ' 

51 56 ' 

5 27 ' 

55 ' 

22 ' 

l. 5 ' 

41 ' 

47 ' 

30'24 ' 

25 46 ' 

34.33' 

26 04 ' 

2 33 ' 

27 49 ' 

28 57 ' 

2 9N 1 b ' 

3C'N1S ' 

3ClN24 ' 

29N08 ' 

27N46 ' 

24 33 ' 

68 'OS ' 

87W13 ' 

8 3w J 2 ' 

8210137 ' 

81W49 " 
Paper 11 

DATA ON COLD WEATHER CONDITIONS ALONG THE ATLANTIC AND 

GULF COASTS DURING THE FALL AND WINTER OF 1976-77 1 

J. Lockwood Chamberlin and Reed S. Armstrong 2 

INTRODUCTION 

The cold weather conditions that prevailed along the Atlantic and 

Gulf Coast during the winter of 1976-77 and the preceding fall 

will undoubteily have significant effects on the marine fishery 

resources and environment. Favorable as well as unfavorable 

effects on re~ource species are, of course, readily conceivable 

regarding their distribution, migration, reproduction, growth, 

and survival. For example, the fall-winter spawning and larval 

survival of some northern species may be enhanced in the southern 

parts of their ranges. Conversely, there may be damage to the 

young of such species as menhaden and white shrimp where they 

overwinter in estuaries. Consideration of possible effects 

should be on a species-by-species and r egion-by -r egion basis, and 

can best be given by the individual scientists who have special 

knowledge of the life histories and physiological requirements of 

t he various ~pecies, and familiarity with the environmental 

conditions in the regions where they work. 

This report presents air temperature anomaly data for selected 

weather stations, in order to describe the severity, duration, 

and distribution of the cold conditions along the entire coast. 

Some discussion of possible effects on estuarine and coastal 

aters is included. 

IThis paper was released in manuscript form as a NMFS Marine 

Environmental Notice, 22 February 1977. Data were derived from 

~~~kly ~~2!h~£ gQQ £~QQ ~~ll~!iQ' Vol. 63 (for 1976) and Vol. 64 

(for 1977), prepared jointly by u.S. Department of Commerce, NWS, 

NOAA, and u.s. Department of Agriculture, Statistical Reporting 

Service; and kQ~21 £iim2!Q1Qgi~gi ~2!2' Annual Summaries for 

1975, Parts I and II, U.S. Department of Commerce, National 

Climatic Center of Environmental Data Service, NOAA. 

2Atlantic Environmental Group, National Marine Fisheries 

Service, NOAAI Narragansett, RI 02882. 
Pap er 11 

ENTIRE COAST COL DER THAN IN PREVIOUS 40 YEARS 

Anomalies of mon thl y mean air temp eratures for July 1976 

J3nuary 1977 app ea r in Fi gur e 11.1 for 12 coastal stations. T

anomalies are based on lon g- term mo nthly means for the 40-

period, 1936 -75. For co mparis on with these anomalie 

Figure 11.1 aLso includes the extremes and standard deviations 

the monthly means for the 40-yr perio d . 

The anamaly data in Figure 11.1 show colder than avera 

temperatures every month from October to January along the enti 

coast except jn southern Florida. Furthe rmore, the record co 

anomalies of the past 40 years are equalled or exceeded in one 

more months at every station except Key We st. At both Savann 

and Jacksonville the negative anomalies equalled or exceeded t 

40-yr record in three of the four mont hs--all but Decembe 

Record breaking anomalies are notable at Atlantic City 

January, Jacksonville in November, and Gal veston in October. 

December, th~ negative anomalies were r elatively moderate alo 

the entire coast. 

Some apparent regional patterns are: 

North of Cape Hatteras, negative an omalies in all mont 

from ~uly to January. 

Hatteras to Jacksonville, negat i v e anomalies in a 

months from August to January. 

Gulf of Mexico, negative anomalies in all months fr 

Octobar to January. 

To permit interyear comparisons of enti re cold seasons, averag 

of the m~nthly mean air temperat u r e anomalies have be 

calculated fo~ the five months, September-J anuary, at six of t 

stations: Portland, Atlantic City, Savannah, Key Wes 

Tallahassee, and Galveston. These averag es a ppear in Table 11 

for the 1976-77 fall-winter period. Al so l i sted in Table 11 

are comparable values for each station f or the four colde 

september-January periods of the previous 40 years. 

The data in Table 11.1 clearly show: 1 ) that record co 

weather conditions prevailed in the fall and winter of 1976- ~lona the entire coast, with the exception o f southern Florid 

and 2) that unusually cold conditions i n earlier years we 

more localized--not extending along the entir e coast. 

Longer records from a few stations (Pro vidence, 1905-197 

rlatteras, 1875-1977; Jacksonville , 1871-1 977; and Galvesto 1~05-1977) indicate that the 1976-77 cold season was unrival 

during the years of record, except at Providen ce in 1917-18. 
Paper 11 

NOTES ON INDIVIDUAL STATIONS 

) portland, ME 

1) All5 months below normal (2nd time in 

also in 1964-65). 

last 41 years; 

2) All 5 months 1 standard deviation below normal (only 

time in last 41 years with monthly means that low for more 

than 2 months). 

3) Record low of 41 years in October. 

4) Average anomalies for 5-mo period, -4.6F (-2.6C), which 

is 1.9 times the previous coldest (1958-59). 

5) December monthly mean colder than normal January value. 

Atlantic City, NJ 

1) All5 months below nDrmal (5th time in last 41 years; 

also in 1969-70, 1968-69, 1967-68, 1962-63). 

2) All 5 months 1 standard deviation below normal (only 

time in last 41 years Nith monthly mean s that low for more 

than 4 months; 4 months in 1967-68). 

3) Record lows of 41 

January. 

years in October, November, and 

4) Average of anomalies for 5-mo period, -7.6F (-4.2C), 

which is 1.3 times the previous coldest (1967-68). 

5) December monthly mean colder than normal January value. 

Savannah, GA 

• 9: 

1) All ~ months below normal (4th time in last 41 years; 

alSo in 1965-66, 1963-04, 1955-56). 

2) Four of the 5 months 1 standard deviation below normal 

(only time in last 41 years with monthly means that low for 

rn 0 ret h an 3 m 0 nth s ; 3 i n 1 9 6 7 - 6 8 ) • 

3 ) R e cor:: d low s of 41 

January. 

years in October, November, and 

4) Average of anomalies for 5-~o period, -5.3F 

which is 1.6 ti~es the pre~ious coldest (1969-70). 

(-2.30, 

5) November monthly mean equivalent to normal December 

val~e, and December mean below nJrmal January value • 
Pap e r 11 

Key west, FL 

1) Three months below normal, Se pt e mber above normal, and 

December no rmal. 

2) unly 1 

(January) • 

mont h 1 standard devi a t ion 

3) No record lows established in 1976-77. 

below normal 

4) Average of anomalies for 

which is J.6 times the 

5-mo period, 

coldest of the 

-1.2F (-D.7C), 

41-yr record 

(1939-40). 

Tallahassee, FL 

1) All5 months below normal (only time in last 41 years). 

2) Four of the 5 months 1 standard dev iation below normal 

(only time in last 41 years with monthl y mean S t hat low for 

more than 3 months; 3 in 1969-7J). 

3) Record low of 41 years in October. 

4) Average of anomalies for 5-mo period , -S. 2F 

which is 1.6 times the previous coldest (196 3-64). 

(-2. 9C), 

5) Novemher monthly mean equivalent to 

value, and December mean below no r ma l 

J1nuary was second coldest of 41-yr record. 

normal Januar y 

.J a nuary val u e ; 

Ga lveston, TX 

1) Four months below normaL (October-Ja nuar) o cc urred 7 

times in previous 40 years; o nl y in 1943-44 were 

temperarures below normal for all 5 mo nths . 

2) Four of the 5 months 1 standard dev ia tion be ow 

(onl' tirre in last 41 years \kith month l y rreans tha t 

'11 0 ret h an 3 m 0 nth s; 3 in 1 943 -44 ) • 

3) Record lows of 41 years in Octobe r a nd Novem be r. 

4) Averdge of anomalies for 5-mo pe ri od· -S. 4F 

w~ich is 2.3 times the previous colde st (1943-44). 

norma l 

low fo r 

5) October monthly mean about equiva len t to nor mal November 

value, November mean below normal Dpcerrber val u e, and 

Dec e m b e r me i::I n below nor rr a L J an u a r y ; J a n I 2 r ,. rr e a n was sec 0 n d 

coldest in 41-yr record. 
Paper 11 

EFFECTS ON ESTUARINE AND COASTAL WATERS 

ID£[~2~~Q ~~[ti£21 mi!iQg: The increased density of 

water will accelerate vertical mixing and alter 

chilled 

normal 

circulation patterns in inshore waters. 

If~ £Q~er: ~ecause the onset of ice cover causes abrupt 

cessation of wind driven vertical mixing, the salinity in some 

estuaries may be above normal near bottom and below normal near 

the surface. 

~~£[~~~~g [~Q~ff: Decreased coastal runoff resulting from frozen 

streams and snowfall, instead of rain, results in general 

elevation of estuarine salinities, although the opposite effect 

can be looked for in the upper parts ~f mixed estuaries where the 

penetration of saLine water alonq the bottom is driven by surface 

fLow toward the ocean. 

l£~ £Q~~[ ~ffe £t~ in £Q~~t~i ~~n~: Ice cover and near freezing 

temperatures in estuaries and lagoons along the southeast 

Atlantic coast, where such con0itions are a rarity, may severely 

affect some resident marine species. Along the northeast coast 

su~h conditions, although normal in the winter, may be having 

marked effects on the marine life because of their unusual 

duration, off&hore ~xtension, and depth penetration. 

~trQDg ~~riDg r~DQff: Wherever there are above normal 

accumulations of snow and ice in the drainage basins, the 

po ssibility exists of strong spring runoff. In the estuaries, 

this would resuLt in an abrupt reversal of the salinity and 

ci rculation conditions that now prevail. On the inner 

continental shelf, strong runoff could lead to early 

s tratificati on of the water column with the possibility of anoxia 

developing next summer, as occurred last summer off New Jersey. 

Despite the a~cumulation of snow and ice in the drainag ~ basins, 

however, strong runoff will stit1-- depend on the volume of 

precipitation during the spring and~iming of the thaw. 

~b~lf ~§l~L tem~~[2t~r~~: Not only should water temperatures be 

expected to equal or go below record low values, but the normal 

spring and su~mer warming cycle may be delayed. Persistence of 

the cold water can be expected, particularly in bottom waters 

over the outpr continental shelf, where the cold water becomes 

insulated from seasonal warming by formation of a warm surface 

Layer. The verticaL stratification may also be stronger than 

usuaL because of coLd dense water persisting at the bottom. 

The AtLantic Environmental Grou~, NMFS, is attempting to 

determine whether the warm Slope Water that contacts bottom on 

the outer continental shelf in the Middle Atlantic Bight could be 

dispLaced in 1977 by abnormally chilled Shelf Water. Such 
Pap er 11 

dispLacemen t nigh t in crease mortality .of .tiLefish and .o:her 

bottom dweLLing animals who s e d ist ri b ut1 0n 1S apparently llm1ted 

to the SLope ~a ter zone, wh ere the t e mperature regime is norma~ly 

quite stabLe throughout the ye~ r. (The weLL-known mass mortaL1ty 

of tiLefish off the Middle AtLantic in ~a rch-May 1882 was not 

oreceded by a cold winter.) 

RECENT REPQRTS OF COLD WEATHER EFFECTS ON FISHERY RESOURCES 

T~e foLLowinQ information has come to o ur attention on the 

~ppar~nt infLuence of the c~ld weather on t he fishery resources: 

~nit~ ~QriffiQ iu ~~~t~ ~~tqiiu~: A newspape r articLe from the 

Uniter Press InternationaL dated February 19 , 1977 reports that 

"CharLes H. Farmer, head of the [South Ca r o l in a] Department of 

~ildlife and Marine Resources' crustacean management program, 

said a week-Long survey showed the cold we ather has virtuaLly 

wiped out the white shrimp that spend the winter along the South 

CaroLina coast." 

~uQQk gUQ Qth~t tc~~i£~l fi~h iu EiQtiq~: Thomas H. Fraser, 

Environmental Quality Laoratory, I~c., Po rt Charlotte, FL, has 

informed us by teLephone that unusually wid espread kiLls of snook 

were reported in Florida during and follo wing the extremeLy coLd 

weather in the third week of January. Other species for which 

kiLls were reported or observed by Fraser du rin g the same period 

of January incLude mojarra, Ladyfish, c r evalle, and tarpon . 

fraser advised that cold weather kiLls ha ve been reported i 

FLorida for each of these tropical species in earlier years. 

C KNOW LE D Glv'l E NT S 

We appreciate the cooperation of LyLe M. Denny, Agricultur ~eather Support Service, NWS, NOAA, washington , DC, who supplie 

us with the WeekLy Weather and Crop Bulletin f o r 1976 and earl 

1977, and Rooert G. Quayle, National Climat i c Center, EDS, NOAA, 

Ashevi Lle, NC, who surpLied the historica L ai r temperature data. 

Donald l. GiLman, NationaL Meteorologica L Center, NWS, NOAA, 

Washinqton, DC, gave advice on sources of dat a. John A. Holston, 

SdPdy Hook Laboratory, Northeast Fisheries Ce nter, first toLd us 

of the snook kiLL in Florida, and ALexander Dragovich, Miami 

a oratory, Southeast Fisheries Center, referre d us to additionaL 

sources of information on FLoriaa fish kills . In the AtLantic 

~n ,ron entaL Grou~ of N~FS, David A. Miz enko and Robert 

• Christ made the statistical caLculations a nd heLped prepare 

t ; ures. 
Table ll.l.--Averages of monthly mean air temperature anomalies (degrees F) for September-January at selected Atlantic and Gulf coast 

weather stations. The averages for 1976-77 are listed for each station. Only the four coldest averages from the previous 40'years are 

listed. 

Atlantic Tal laPortland City Savannah Key West has see Galveston 

1976-77 -4.6 -7.6 -5.3 -1.2 -5.2 -5.4 

1970-71 -2.2 

1969-70 -3.8 -3.3 -2.5 

1968-69 -3.3 -1.9 

1967-68 -5.9 -2.9 

1963-64 -3.1 -1.6 -3.3 

1961-62 -1.4 

1960-61 -2.2 

1958-59 -2.4 -2.9 -1.5 

1956-57 -2.4 

1955-56 -2.4 

1954-55 -1.7 

1943-44 -2.7 -2.3 

1939-40 -1.9 -1.8 

1937-38 -1.6 

173 
u.J 

U 

Z 

u.J 

o 

.... 

> 

o 

a: 

~ 

u.J 

-' -' 

> -

VI 

z 

31: 

o 

a: 

m 

+10 

+ 5 

JUL AUG SEP 

.................. .. ........ 

OCT NOV DEC 

... .. .. .... .... .. .. .. 

-- - - .: :.:. .- ----

JAN 

° +----...-----,..-- -.-:- - -1- - 5 

-10 

...... .. ... .................... " .. 

.. ............ .. 

i . ooOO oo .. oooooo .. oooo ................ .. 

+ 5 •••• ____ ----------- ----

OJ L ---'-;i;-=--~---=-=-------.-;-=-=-~ ----.--1-------.1------'-1"---- 1--~ 

............ 

- 5 ...... , ............... ' '. . ....•... 

-10 .•.••• . ' . + 51 ........ 

~1 0~ :"-' -= ..: :,,'- - - - - - - - - - - - - - - - - -- '!-.-;-;-.-:-I-::-.--I---- ___ _ ........ . .. 

-l~ ........... ~._. ____ _ - --- -- - O+-~_~. ~~~~~.-=.~~--~------.----~--or----r--

- -- 5~ '. --- J .. '. : • .. . " 

~ + 5 ------- --- > 0 +---._~_~_~_~~~--.r-----,r------r-----,~ 

-' - 5 ~ 

E -10 

1 

.......... 

.......... 

.. ----- - -- ---

1 ................ - -1-- --1- -:--:.---- I t .......... 

::::J + 5 .................. .. L ~ l+---·~==-.~:,;·;.:: ::::::--=.:::::' .-::.::.. ..,;j;..:. ~ ~: ~ \~7~ : : ~-; ; ~ ; ~ ~ -

: • :5t--~~~~~·~·~r~r~.~~=-.~~~~.~·~·-·--·-'·r~--·--·-~---.-~--.--.-~--~--- ~ :-. -;' -;- -:- :-. --;- -:- ~ ~ .-' 

~ :

'

: t-=--=--=-=-=:-==-:'-=':::' "':'::-r.:':" -==-' '--' - -.-..:.. ~-:"-' ~ ...--~ .:.-~---..~ ~.---~ -"-' ---. . .:---

-5 '· •. -:-I---l- .. .. .. .. .. __ ~_ --t 

-10 ••••• : : .... 

.. .. .. .. .. .. .. .. 

+ 051+- ~ __ ~~~~~~~----.;"r·=-·-=-=,_;.-------,-r_-----~- ....... _ . ....: ..:...-

:,~j' 7 ... • .-.-+:~:_+~:-+.-- ~ 

.. + 055~~..-----r· •..•. __ ..•• " . _____ " 

I .-. ~.-.. ~ -'- ... '-'-=':" '-'- - - --- - - - -- 1 ........". -1- ---1---=1- - I .... .. .. .. .. .. .. .. -- .......... 

~:5t-i·~·~·~·~~~~~~~·-·-·-·-· ·r·-·-·--,,---:-: :--- I . .. ~ , :~ ~ ~:~ ~ ~ ·~ ~.~ ~ -:I-:~---- ~ ~ = -- -10 • • •• . • . • 

174 

I ANOMALY FOR 1976/77 

MAXIMUM AND MINIMUM 

VALUES FOR 1936- 1975 

- - - ! 1 STANDARD DEVIATION 

FOR 19 36- 1975 

Figure Il.l.-Anomalies of monthly mean air 

temper atures at selected Atlantic and Gulf 

coast wea ther stations, July 1976-January 

1977, based on long-term monthly means for the 

40 years, 1936-75. Shown for comparison are 

the maxima and minima and standard deviations of the anomalies for the same period. 
Paper 12 

WIND DRIVEN TRANSPORT 

ATLANTIC COAST AND GULF OF MEXICO 

Merton C. Ingham l 

INTRODUCTION 

ariations in surface currents and transports resuLting from 

hanges in the overLying wind fieLd are significant factors in 

he survivaL and development of the early stages of several 

esource species and the strength of year classes of their 

opulations. This is especially true for species whose Larvae 

pend a relatively lonq ~eriod of time as plankton in the surface 

ayer. 

n exampLe of the influence of wind driven transport on larval 

urvival, recruitment, and year class strength can be found in 

he Atlantic menhaden. Winter spawning of this species takes 

lace south of Cape Hatteras at some dist ance offshore, near the 

dge of the Gulf Stream. Eggs and larvae from this spawning 

ctivity are transported toward estuarine nursery grounds, under 

avorable conditions, by wind driven currents in the surface 

ayer. Studies of monthly Ekman (wind-driven) transport and 

ecruitment fo.r the years 1955-70 have revealed a strong link 

etween years of high or low recruitment and years of strong or 

eak westward Ekman transport during January-March. A model 

eLating these factors shows that variations in January-March 

onal Ekman transport at a point south of Cape Hatteras accounts 

or about 60% of the variation between actual and expected 

density-dependent) recruitment (NeLson et ale 1977). 

n addition to the effect of wind driven transports on Larval 

frift, there are other reasons for scientific interest in the 

ariations of Ekman transport: 

-----

lAtLantic EnvironwentaL Group, National Marine Fisheries 

ervice, NOAA, Narragnasett, ~I 028b2. 

1L5 
Paper 12 

1. Coastal upwelling, which is quite 

Pacific coast, is c consequence of 

this type and can occur along any 

appropriate wind stress. 

prcnouncea aLong the 

offshore transports of 

coastline, given the 

2. Coastal circulation patterns, such as those described by 

Armstrong - for the western Gulf of Mexico, are strongly 

influenced by variations in Ekman transport. 

3. The position of water ~asses and their ~oundaries, sue 

as the Shelf WaterlSL~pe Water front along the Atlan tic 

coast, are influenced by wind driven transports. As a 

consequence, the distribution of peLagic fishes aLso may be 

influenced because many of them tend to associate with 

particular water masses, especially in frontal areas. 

4. The efficiency of productivity cycles and their timing 

in a particular location may depend a great deaL on the 

presence or absence of specific water masses, whose movement 

may depend largely on wind driven transrort. 

The data portrayals presented here are drawn from among the suite 

of parameters computed from monthly average pressu re distributions. 1 Figures 12.1-12.4 graphically display mean monthly Ekman 

transport values for 1976 and f~r a 10-yr base period, taken from 

an alternate 5-deg grid for the Atlantic and a 3-deg grid for th e 

Gulf of Mexico. Table 12.1 contains the corresponding zonal and 

meridional transport values. 

I n order to provide a more complete set of data for studies 

areas not well represented by the locations selected 

Figures 12.1-12.4, the 19 76 me an monthly and 10-yr monthly mear 

zonal and meridional trans~ort values for all points on the 3-de. 

g rid in the mapped areas are portrayed in ~ppendix 12.1. 

2Armstrong, R. S. 1976. 

s alinity and circulation. 

Te xas Outer Continental 

Oceanography, p. 43-51. 

Galveston, TX 77550. 

Seasonal cycle of temperature, 

In Environmental StUdies of the Soutr 

Shelf, 1975, VoL. II, PhysicaL 

GuLf Fisherles Center, NMFS, NOAA, 

D~ta provided by Pacific Environmental Group, 

Fisheries Service, NO~A, Monterey, CA ~394~. 

National Marine 

176 
Pa~er 12 

DISCUSSION OF 1976 CONDITIONS 

~!12Q!i£ (Figs. 12.1 and 12.2) 

Significant anomalous conditions are revealed in the 1976 record 

of mean monthly Ekman transport for both 35N, 75W and 40N, 70W 

during the early months (FebruarY-March) and the late months 

(November-December). During February and March the transports 

were to the southeast instead of to the southwest, produced by 

winds from tbe southwest instead of the northwest. The eastward 

component of Ekman transport was larger than for any other 

February in the 31 years of record. Only one other February in 

that period (1971) showed eastward transports, and it was about 

one-half that shown in 1976. These anomalously persistent winds 

from the southwest, especially in February, brought with them 

much warmer and more humid air than usual and very few storms 

offshore. This condition yielded unseasonably mild weather and 

high river runoff along the coast and apparently led to unusually 

early stratification over the shelf (Armstrong, Paper 17). 

Another possinle impact of the unusual southeastward transports 

in February and March is the loss of larvae of several commercial 

species from Georges Bank, located immediately northeast of 40N, 

70w. Once transported off the Bank to the southeast the larvae 

would be in a more hostile, deep-water, pelagic environment and 

probably would be permanently lost from the year class. 

During November and December at these two points the transports 

were toward the southwest, in agreement with the 10-yr average 

conditions, but their magnitudes were unusually large. The 

persistent, strong northwesterly winds which produced these unusually large transports brought with them the cold temperatures 

of the continental air mass, yielding the record breaking severe 

winter experienced by the east coast (Chamberlin and Armstrong, 

Paper 11). Here again, as was the case in February and March, 

the unusual transports shown at 40N, 70W reflect conditions which 

could have caused significant transport of planktonic organisms 

away from Georges Bank. Fish larvae from the year class 

developing on the Bank at that time and still in the planktonic 

stages would suffer losses. 

The anomalous transports which occurred in the vicinity of 35N, 

75W in February and March should have had an impact on the 

transport of menhaden larvae spawned offshore south of Cape 

Hatteras in the January-March period. The eastward components of 

the transports would tend to transport the larvae offshore, away 

from the estuarine nursery areas they require for development. 

That portion of the spawning, and larval transport which occurred 

in January, when there was a westward component in the Ekman 

transport, should have been more successful. 
Paper 12 

In the vicinity of 30N, 80W, an area of considerabLy smaLLer 

Ekman transports, the most unusuaL condition in 1976 was the 

relatively strong northeast~ard transport in June. Such transport shouLd have resulted in some upweLling along the Florida 

shelf. During July the transport shifted to southeastward and 

was stronger farther north, at 35N, 75W, which couLd have 

produced u~welling on the sheLf off Georgia and the caroLinas. 

§~lf Qf ~~~i£Q (Figs. 12.3 and 12.4) 

The most apparent departure in 1976 from the 10-yr mean conditions in the GuLf of Mexico was the strong northwestward 

transports du~ing the October-December period. These transports, 

which were more westward than normal at alL three of the 

positions portrayed, are the consequence of unusuaLLy strong or 

persistent northeasterly winds during the early part of the 

severe winter of 1976-77. These conditions shouLd have produced 

unusually strong onshore and counterclockwise alongshore fLow. 

During January the difference between the transport vectors at 

27N, 96W and 27N, 90W, which usuaLLy produces countercLockwise 

nearshore circulation in the western Gulf (see footnote 2), was 

greater than normal. This condition should have Led to mor.e 

intense nearshore flow to the west and south <counterclockwise). 

In February and March the difference in transport values between 

the two positions reversed, with the stronger vaLue at 27N, 96W, 

including a strong east~ard component. This may have caused a 

reversal in nearshore circulation, to clockwise, during February, 

a month earlier than normaL. 

LITERATJRE CITED 

NELSON, ~. R., M. C. INGHAM, and W. E. SCHAAF . 

1977. Larval transport and year class strength of Atlantic 

menradenl ~[~~2Q[ti2 t~[2QQi~. Fish. Bull. u.S. 75:23-41. 

178 
Table 12.1.--Monthly average Ekman transpor t s for selected points off h 

coast and in the Gulf of Mexico f or 1976 . Units are t/s-lan . Positiv 1 

or northward. 

Jan Feb Mar Apr May Jun Jul 

40 oN , 700W 

Zonal -70 170 30 - 90 240 180 110 20 20 - 20 -200 -1 

Meridional -220 - 700 - 190 - 270 - 290 - 260 - 250 - 70 - 90 - 0 - 0 -

~2oN z 72°W 

Zonal -60 130 80 - 50 180 170 100 10 0 -50 -... 90 -100 

Meridional -170 -440 -140 - 80 - 90 - 30 - 290 30 0 30 -)10 - 8 

30oN , 800w 

Zonal -60 10 100 - 10 190 180 80 40 10 -150 -180 -1 

Meridional 20 - 20 30 20 20 140 - 110 160 80 210 60 

21~ z 8i±OW 

Zonal - 270 -30 220 - 30 220 100 20 - 10 10 - )80 - 80 -

Meridional 500 170 430 190 70 260 10 160 110 650 720 

nON, 900w 

Zonal - 340 -10 520 80 30 100 10 - 1)0 - 60 - 520 - 0 -

Meridional 780 260 960 630 230 550 160 210 2)0 770 0 

27~, 69°W 

Zonal 20 410 530 1000 210 500 790 190 120 -2 0 -6 

Meridional 450 330 1110 1140 510 790 890 )20 70 620 
Paper 12 

In the vicinity of 30N, BO W, an area of considerably smaller 

Ekman transports, the most unusual condition in 1976 was the 

relatively strong northeast~ard transport in June. Such transport should have resulted in some upwelling along the Florida 

sheLf. During July the transport shifted to sout heastward and 

WaS stronger farther north, at 35N, 75W, which could have 

produced u~welLing on the shelf off Georgia and the carolinas. 

§~lf Qf ~~~i£Q (Figs. 12.3 and 12.4) 

The most apparent departure in 1976 from the 10-yr mean conditions in the Gulf of Mexico was the strong northwestward 

transports du~ing the October-December period. Thes e transports, 

~hich were ~ore westward th an normal at all three of the 

posit"ons portrayed, are the consequence of unusually stFong or 

persistent northeasterly winds during the early part of the 

severe winter of 1976-77. These conditions should have produced 

unusually strong onshore and counterclockwise along shore flow. 

During January the difference between the transport vectors at 

27N, 96W and 27N, 90W, which usually produces coun terclockwise 

nearshore circuLation in the western Gulf (see footnot e 2), was 

greater than normal. This condition should hav e led to mor.e 

intense nearshore flow to the west and south (counterclockwise). 

In February and March the difference in transport values between 

the two positions reversed, with the stronger value at 27N, 96W, 

including a strong eastward component. This may have caused a 

reversaL in nearshore circulation, to clockwise, during February, 

a month earLier than normaL. 

LITERATJRE CITED 

NELSON, w. R., M. C. INGHAM, and W. E. SCHAAF. 

1977. LarvaL transport and year class strength of Atlantic 

menhadenl ~[~~~Q[li~ l~L~DQi~. Fish. BuLL. u.S. 75:23-41. 

178 
Table 12.1.--Monthly average Ekman transports for selected points off the U.S. east 

coast and in the Gulf of Mexico for 1976. Units are t/s-lan. Positive is eastward 

or northward. 

Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec 

40 ON , 700

W 

Zonal -70 170 30 -90 240 180 110 20 20 - 20 -200 -130 

Meridional -220 -700 - 190 - 270 - 290 -260 -250 -70 -90 -40 -760 -470 

35 ON , 75°W 

Zonal -60 130 80 - 50 180 170 100 10 0 - SO -190 -100 

Meridional -170 -440 -140 - 80 - 90 -30 -290 30 0 30 -310 -180 

30oN, 800w 

Zonal -60 10 100 -10 190 180 80 40 10 -150 -180 -120 

Meridional 20 - 20 30 20 20 140 -110 160 80 210 60 60 

27°N z 8~OW 

Zonal - 270 -30 220 - 30 220 100 20 -10 10 - 380 -480 -260 

Meridional 500 170 430 190 70 260 10 160 110 650 720 570 

27°N, 900W 

Zonal - 340 -10 520 80 30 100 10 -130 -60 -520 -740 -450 

Meridional 780 260 960 630 230 550 160 210 230 770 1020 720 

27°N, 69°W 

Zonal 20 410 530 1000 210 500 790 190 120 - 240 -680 -480 

Meridional 450 330 1110 1140 510 790 890 320 470 620 880 520 

179 
• • 7 • W 

JAN 

MONTHLY 

Figure 12.1 -"!l'an monthl) Ekman trun port 

180 

MA 

197 

4 • 

c 

• 

TI A NIPOIT 

t r r 
80° 

80° 

JAN DEC j711 \~ '1/ 

! , ! I I , , I , I ! 

IOOOM£rRIC 'rONS / s£c / KM 

MONTHLY EKMAN TRANSPORT 

10 YEAR MEAN 

1964-1973 

Figure 12.2.-Mean monthly Ekman transports for three representative points off the U.S. Atlantic coast for the 

10-yr period 1964-73. 

181 
I ur 

• 

ONT 

TRAN 

197 

o· 

2 • 

A 

o T 

1 2 
MONTHLY EKMAN TRANSPORT 

10 YEAR MEAN 

1964-1973 I I I I I I ! I I I I 

1000101£ TRIC TONS / SEC / Klol 

Figure 12.4.-Mean monthly Ekman transports for three representative points in the Gulf of Mexico for the JO-yr peri()d 1961 -7:1. 

1 
APPENDIX 12.1 

Mea~ monthly Ekman transports (t x 1G/kw-s) 

in the western North AtLantic and the Gulf of 

Mexico for 1976 (upper numbers) and for 

196~-73 (lower nu~bers). Left numbers are 

zonal (positive eastward) and right numbers 

are meridional (positive north~ard). 

1M 
J.~~UARY 

-1~-f22 -2!t--30 -~-f32 llt-!!l 

-27 -52 -3~ -43 -42 -25 -53 -14 

-1~13 -7~29 11f=47 3~-57 

-25 -41 -39 -17 -61 -3 -83 7 

5 ° 

o 

-18+24 

16 -6 -~+10 

10 -3 

-1+6 

12 -0 ~+10 12 1 6~/~ 

9 3 

7+17 

7 ? 

o 25° 

H-~7 ? -11 

80° 75° 70° 65° 

185 
80° 

4 

FEBRUARY 

. '.: .. :.... 16+"7') 17 -f67 22 -f"F)7 . . . :,' ": . .?1 0 -3 6 -14 -2 4 -If) -12 • • • ,,', . ,."_ ... 1 ", 

4 

, 

3 

.-" lL: 31 10J - 31 1 r:Lc32 12 -f"3'1 17 1-33 ?S +"41 

.', ,t' -81:20 -14'=-23 -3/f'-12 -5q 9 -6tT~3 -7ft 27 

31 

-4+17 -hJ1 -fh1,) O-.ll2 5+15 11~11 2 -3 -~1-1 _/1) -91) -12 7 -12116 

-2~1023 -16~16 -7 98 -13 64 -9 59 327+164 

rrr 5 I~ 54 +-6 143+-3 4~ ~o 31 11 

2 

186 
o 

° 

~ ° 

5 0 , 

80° 

MARCH 

80° 

1~1 

-10 1 

16+.8 

8 5 

-~-F12 -~-17 -~1F16 -1+:19 

-17 -20 -21 -20 -23 -12 -35-5 

7+0 leI ()~J '±J..:-12 16-f19 

-13 5 -18'11 -23112 -2Sr-9 - -31 7 

7~7 

1 2 ~9 ~1 3 1 ~ ~3 1 -1 

0-i6 

34 ? 

7 5° 70° 65° 

187 

25° 
APRIL 

- 3---L22 

20'8 -~IQ 

IST3 

~T3 

-9 -9 

-ID -4~ -6 -47 1 -42 9 -37 

-aJ1--9 -14+:15 -141C13 -1i+=7 

-7~1 -hl 

-11'3 -19'J. 

-~6 -~ 15 -0 13-2 

188 

1 ? 11+3 

';4=9 -51 13 

3i2 

10'= 1 

4 , 

4 
MAY 

45 --.C44 4Qc41 

-121 5 -16' 8 

1

0 40 0 

) 0 

o 

2~28 3~-36 4~~35 3~35 

-T1 3 -91 6 -13 10 -21 17 

. ' .......... :.::\'/ 1~- 11 32lf21 41+--29 42+31 41+="31. . ..' .';;, -5 5 -ICl 9 -16 17 -26 27 -36 35 . . . .: .".::". 

5~1E17 4~-2 0 4~22 3~-[9 

-12 24 -17 30 -21 33 -22 32 

38-t:4 5~- 4 5?-t3 4~-1 3~2 1~1 

4 14 3 21 4 22 5 22 8 21 10 16 

189 
JUNE 

1*--14 2~27 32-f39 2~-fS4 

-11 10 -14 16 -17 21 -22 25 

3~-11 4~4- -21 3~ 24 311F33 

-9 15 -12 21 -16 26 -21 33 

. . '. : .. :>/ 1~5 2~ 48-+.2 4~-t4 34-+-6 25-E7 . :~~. ~ 7 -1 14 -4 20 -5 25 -9 30 -11 35 . ': : ~. '.: . 

. . : 

3~ 46 4~~7 5~66 5~8 35 -{{ 2,)~5 lar21 19 23 23 25 23 7 24 _6 29 23 

190 

3 

2 
JULY 

o 

° . , 

o 31 .... 43 44 I-53 q~1 -51 35x 4rJ ~6~"31 2~L':1-)7 

-~2 -~3f) -~31 ~26 3~1 ~ 

15 3 18 "3 1~-1 ~1 51? 5 1 

2f)-ir8 24~21 27 21 30 1>3 ~7 fj 414r2 

50 25° 

1iti9 5~ 4 I·m , 9 1a8 113-+9 

80° 75° 70° 65° 

191 
AUGUST 

7 -13 10 -17 1~ - ~ 

19f- g -2 11+ 12 -36+ 17 

40 0 4 

o -5 ~-1 11+- 1 1~17 

-6-rS _1T -IS 15 -2~1 21 

.. ... 1J S+') q+-~ 1~ - l~S 

. ',- -3'4 -7 1~ -14 20 -iT2 -?8')/l 

~o 1 12 

~ ') Il,-+~ 

-S IS -10 27 

1~16 

4 20 

1#-14 

f IS ~-¥,3 lQ 11 

11-#7 1~?2 2~)1 1~-#7 ~5 ?-#4 

21 17 22 18 29 18 32 1/f 36 1') '12 8 

192 

3 

3 

2 

35° 

OCTOBER 

-S-t:.3 o 0 1 0 

13 15 1:fP-S g~1 

...... ·:)"·-17. 13 -14J-l -3+5 ') 3 ? 1 

.' . '. : .. ;.::r: .... :. 4T -33 .. " . - 32 -21 2'1 -6 1~2 16-tl 

:. l 29 -2~3 -IW4 -2+11 w.3 9-tl0 .. ~ -29 38 -24 26 -3 24 1 23 ~ ~2 1 

-2~ 49 -12 21 -3 IS S 24 

S!J-14 33+-6 31+-1 32-+2 

194 

~+"1 6 1 

'-H1 13 ~ 

6 g 

21~ 

4

2 
, 0 

° 

o 

50 

NOVEMBER 

. ,',:': '.: 

. . . .. .. :'.:'." -33 -86 -17 -8q . ' .. ";'. ~ if- . . . ':'.:' .. ::. 9 10 8 11 . . " ... :::.:-.:.:,, - - -- . :;'.; :::::::.," .. .. ' 

2 -92 

-8+-9 

-4~ -69 -34 -77 -9 -78 14 -86 

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Far·er 13 

SEA SURFACE TEMPERATURE DISTRIBUTION FROM 

CAPE COD, MASSACHUSETTS, TO MIAMI, FLORIDA - 1976 

Joseph W. Deaver III I 

Since July 19b9 the U.S. Coast Guard Oceanographic Unit has been 

condu~tin g mQnthly airborne radiation thermometer (ART) surveys 

of the U~S. Atlantic coastal waters (Deaver 1975). These surveys 

locate oceanographic features such as the surface Siome (convergence streak lines) associated with the Gulf Stream, define the 

sea surface temperature (SST), and report marine animal and 

poLlution siqhtings from Cape Cod, MA, to Mi3mi, FL. Data 

collected in 1976 were obtained over 6,800 km of transects 

covering approximately 130,000 sq km of Atlantic Shelf and Slope 

Waters. The resu lts of the monthly surveys from January through 

December were distributed within several weeks after each survey 

(Appendix 13.1). 

In 1976, the &pring warming trend began from Miami to Cape 

Hatteras during February and ~arch, one month earlier than in 

1974 (no data were available for this area in early 1975). North 

of Cape Hatteras, to Cape Cod, the spring warming began during 

March and Apri l 1976, about one month earlier than in 1974 and 

1975. The SST patterns stabilized in all areas between July and 

September 1976. In 1974 and 1975 the summer patterns were 

stabilized for only two months, July and August. A rapid fall 

cooling trend extended from Cape Cod to Miami in September and 

October 1976. This strong cooling trend lowered SST's an average 

of 5C in less than 30 days. The rate of cooling began to 

diminish between Miami and Cape Hatteras during October and 

~ovember but the trend continued from Cape Hatteras to Cape Cod 

until late November. In 1~74 and 1975, the cooling trends were 

more graduaL, beginning in August and September and continuing 

untiL late DeJ:ember. 

An'alysis of the 1976 ART data was made by comparing them to a 

SO-yr (1914-64) historical average (Walford and Wicklund 1968). 

ALthough the ~omparability between remoteLy sensed and bucket 

-----

I U.S. Coast Guard Oceanographic Unit, Navy Yard, Washington, DC 

20590. 

0/10 
Pap er 13 

gat hered temp er a t ures might be questio ne d, it is still of 

interest to make such a co mpariso n . The difference between lo~ 

altitude ART and bucket temperatures is sma ll; ART temperature s 

averaged 1.0C lower than bucket values , a nd 95% of ART value s 

were O.3C to 1.SC lower tha n bucket values. Comparisons between 

ART observations on Coast Guard aircraft a nd surface trut h 

measurements have shown differences of less tha n 1C. 2 

For both the 1976 ART data and walford and Wicklund' s (1968 ) 

data, a monthly, distance ~eighted, mean t r a ns ect SST wa s 

calculated for each of 20 equally spaced sam plin g transects from 

Care Cod to Miami (Fig. 13.1). The samp ling transects were 

aligned normal to the 180-m isobath and the shoreline 

(Fig. 13.2). The weighted means are g i ven in Tables 13.1 and 

13.2. The means from the 20 transects were a v e r ag ed to give the 

mean east coast SST for each month (Fig . 1 3 . 3 ). The monthly 

means were than averaged to give an annual me an e ast coast SST. 

The 1976 annual mean east coast SST averaged just 0 .6C below the 

historicaL annual mean SST of 19.0C ( Fig . 1 3 .3). In 1976, 

J a nuary, February, and September-Decembe r SS T's were belo~ 

historical averages. Conversely, the remaini ng s p ring and summer 

months were sLightly warmer than the histo r i c a l average. 

In addition tQ the comparisons for the en t i re east coast, the 

Middle Atlantic Bight winter and summer tem~eratures were 

compared. This was Gone by averaging the monthly distanc e 

weiqhted mean transect SST's for transec ts 14-19 (Fig. 13.2) t o 

obtain monthly Middle Atlantic 3ight SST 's. The January-Marc h 

and July-September monthly Middle Atlant ic Bight SST's were the n 

averaged to give seasonal winter and su mme r means for both th e 

1976 data and walford and Wicklund ' s (196b) data. The winte r 

1976 SST in the Bight was 5.6C, which is 0.3C cooler tha n 

historicaL averages. Interestingly, the July-September 1976 mea n 

east coast SST's were O.1C warmer than th e historical averages, 

as were the 1976 mean Middle Atlantic 8 i g ht values. 

The warmest monthly distanc e weighted mean transect 

east coast in 1976 ~as t r an s e ct 1 off Mi ami, FL, in 

value of 29C; the coolest was t ra n sect 20 off Cape 

March with a value of 3.8C . 

SST off t h 

August wit h a 

Cod, MA , i n 

2Pick e t , R. L. 1966. Accuracy of an airborne infr are d 

ra di ation thermometer. u. S . Naval Oceano g raphic Off i ce, In forma ~ 

Manuscrip t Report No. 0-1- 66 . 

0 1A 
LITERATURE CITED 

DEAVER, J. W. 

1975. Aerial oceanographic observations, Cape Cod, 

setts to Miami, Florida, July 1969-June 1970. 

Guard Oceanogr. Rep. CG 373-68, 27 p. 

WALFORD, L. A., and R. I. WICKLUND. 

Paper 13 

Massachuu.s. Coast 

1968. Monthly sea temperature strJcture from the Florida Keys 

to Cape Cod. Sere Atlas Mar. Env;r., Am. Geogr. Soc., 

Folio 15, 16 plates. 
Table 13.1.--Distance weighted historical mean sea surface temperatures (degrees C) at 20 

transects off the U.S. Atlantic coast; calculated from Walford and Wicklund (1968, see 

Fig. 13.1). 

SECTION JAN FEB MAR APR MAY JUN JUL AUG SEP OCT NOV DEC 

1 22.5 22.5 22.5 25.0 25.0 27.5 27.5 27.5 27.5 27.5 25.0 22.5 

2 23.0 22.5 22.5 23.9 25.0 26.6 27.5 30.0 27 .5 26.3 24.8 23.2 

3 22.0 20.6 21.8 23.1 23.8 25.8 26.7 26.4 27.5 25.0 24.5 22.5 

~ 4 19.0 19.9 19.6 21. 4 24.4 25.4 26.6 27.3 27.5 25.0 23.3 21. 5 

5 18.4 18.9 19.8 21.1 23.0 25.4 27.2 27.5 27.5 23.8 21. 2 20.4 

6 15.9 17.3 18.4 21. 0 21. 0 25.9 27.5 27.5 27.5 23.8 19.9 18.2 

7 15.0 15.7 17.0 18.7 21. 9 25.3 26.3 27.5 27.0 21.0 20.2 16.3 

8 17.5 16.6 17.0 17.1 22.5 25.0 25.8 27.5 26.0 22.3 19.0 16.9 

9 15.9 15.6 16.5 18.4 21. 2 25.0 27.0 27.5 25.9 22.1 18.4 18.0 

10 17.6 13.8 15.7 20.8 22.5 25.0 25.0 27.5 26.5 21.5 19.0 18.4 

11 14.5 17.8 15.6 19.4 21. 3 23.0 25.5 25.9 25.3 21. 9 18.7 17.0 

12 18.6 19.2 17.5 20.0 22.0 25.0 27.3 25.0 25.6 23.4 17.9 16.9 

13 15.9 13.0 11.3 20.0 19.5 22.9 23.8 25.3 25.0 21. 3 18.6 15.0 

14 8.1 7.3 8.1 10.5 15.0 20.0 23.4 24 . 3 23.1 17.9 15.0 11. 7 

15 7.7 6.0 4.1 7.1 12.5 18.1 22 . 5 22.5 23.5 17.5 14.1 9.8 

16 5.9 5.0 7.0 8.2 10.4 15.7 21. 6 23.3 22.1 19.8 15.9 10.2 

17 5.4 6.3 4.6 7.5 10.6 15.5 20.8 22.2 20.5 16.1 13.7 9.5 

18 7.6 4.7 4.1 5.3 9.5 14.3 20.0 21.6 20.3 16.5 12.3 8.9 

19 6.4 4.5 3.0 5.5 8.7 12.9 18.8 21.3 18.7 15.0 12.7 7.9 

20 3.1 4.2 3.4 5.2 8.6 14.7 16.3 20.6 19.4 15.0 12.9 9.3 
Table 13.2.--Dista nce weig hted 1976 mean sea surface temperatures (degrees C) at 20 transects off U.S. Atlantic coast; c alculated from monthly sea surface temperature charts (see 

Figure 13.1). 

SECTION JAN FEB MAR APR MAY JUN JUL AUG SEP OCT NOV DEC 

1 22.0 22.0 24.0 24 .0 25.0 27.0 2S.0 29.0 2S.0 25.0 25.0 22.2 

2 22.4 20.7 24.0 24. 0 26.0 27.0 29.0 2S.5 2S.0 23.7 24.4 22.5 

3 19.3 17.9 22.0 23 . 2 24.3 25.6 27.9 2S.0 27.4 23.2 23.1 20.2 

4 17.3 lS . l 20. 7 23 . 3 24.5 25.5 2S.0 2S.0 27.0 23.0 22.1 19.3 

5 17.S 16.9 20. 5 22 . S 23 .0 25.5 29.0 26.0 21. 4 19.2 16.S 

6 14.5 13.8 lS.7 23 . 2 23.3 24.7 29.0 25.6 20.3 lS.5 16.S 

t,:) 7 13.4 12.S 17.6 21. 6 23.7 24.3 29.0 25.5 20.4 lS.2 16.S ...... 

w 8 13.1 11. 8 16.7 21. 2 22.4 24.0 2S.5 25.5 19.8 lS.9 17.6 

9 14.5 12.1 16.4 20.9 22.0 23.3 27 .4 24.S 19.7 17.7 16.0 

10 12.8 12.S 17.6 21.1 22 .2 23.9 27 .0 26.6 25.6 21. 0 lS.6 17.8 

11 12.6 11. 5 16.2 20 .7 21. 7 23.0 27.0 26.5 25.3 19.8 16.S 

12 13.3 12.9 15.5 20. 7 21. 9 22 .9 26.6 25.3 19.8 14.6 

13 6.0 14.S 9.4 19.6 20.4 19.3 28.0 23.5 lS.4 13.1 14.1 

14 6.0 8.0 8.6 12 . 9 16.3 19. 4 24.0 23.0 18.3 12.7 9.5 

15 4.4 6.2 6.2 12.4 13.1 17.3 23.0 22.6 23.0 16.9 10.8 9.2 

16 4.7 5.8 5.6 11. 3 13.5 lS.0 23.3 21. 7 21. 8 14.4 9.3 8.1 

17 4.8 5.0 5.3 12 .0 12. 7 16 .4 21. 0 21. 0 14.7 9.6 7. 2 

18 4.6 5.3 5.3 10.9 11.6 16 . 3 17.9 19.6 14.0 10.1 9.1 

19 4.8 5.2 4.4 8 . S 11. 4 15.8 l S. 3 20.1 13 .9 10.6 

20 3.9 4.1 3.8 8 . 3 9 . 5 13 . 3 18 .5 19.0 14 .0 S.4 
if = 

'vhe r e : T -

T' 1 -

t· - 1 

n -

i=l, n 

i= l , n 

e.·T· 1 1 

is tance wei 1hted mea 

oerature 

Value of 

transect 

an isot.erm 

t emr o ssi n 

~ista ce facto r 

_ ual to t ~ 1i ~a ces bet ee n 

t~e iS0therm ss in~ a~ ~ e 

~idooints between it an a dj a-

:~nt isot'1erms o r i t and the end 

~oint of the t r an s ec t a s shown 

1. :iqure be ow 

, :'TIber 0: iso 

the transerts . 

• • 

• • 

e rms c rossing 

• • 

• • 

Figure l3 .1.- Formula and graphic portrayal of method used to calculate distance weighted mean sea surface 

tempera ture from contoured isotherm chart. 

214 
80° 

Washington 

... 

80° 

.. . -.- .. 

14 

. 

. 

....... ;~ . 

. ...... 180 Meter Isobath 

Figure 13.2.-Standard airborne radiation thermometer sampling transects from Cape Cod, MA, to Miami, FL. 

215 
U 

0 

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a:: 

:::> 

..... 

~ 

a:: 

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Q.. 

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..... 

26 

24 

22 

20 

8 

16 

14 

12 

10 

1976 ANNUAL MEAN EAST COAST SST 18 4° C 

HISTORICAL ANNUAL MEAN EAST COAST SST 190° C 

~.-• . ;; 

I·~ \. 

\' /, 

. , 

/.,' 

. / 

/ " 

/ 

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• 

• 

, 

, 

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1976 MEAN EAST COAST SST 

(USCG ART FLIGHTS) 

HISTORICAL EAST COAST SST 

(WALFORD. WICKLUND) 

'. 

• 

JAN FEB MAR APR MAY JUN JUL AUG SEP OCT NOV DEC 

MONTH 

Figure 13.3.-East coast average mont l~ mean ,ea urfnce tcmperatu rl' ( Tl {degr ,( I for Ill,!; a nd the h"lorlca l \ raKe. 

216 
APPENDIX 13.1 

Sea surface temperatures (degrees C), 

U.S_ east coast, as observed by airborne 

radjation thermometer. 

1. January 20-24,1976. 

2. February 10-12 and 20-24, 1976. 

3. March 11-12, 14, and 23-25, 1976. 

4. April 20-22, 1976. 

5. May 18-21, 1976. 

6. June 8-10, 1976. 

7. July 20-22 and 27-28, 1 976. 

8. Au~ust 17-19, 1976. 

9. September 14-17, 1976. 

10. October 19, 21, 22, 27, 28, and 30, 1976. 

11. November 16-20, 1976. 

t2. December 8-10 and 14-16, 1976. 

217 
DEPARTMENT OF TRANSPORTATION 

I.S. CUST CUll OCEUoumlC UIT 

lirhr .. h~iltill a.r •••• t.r Pr'lll. 

SURFACE ISOTHERMS· °C 

JANUARY 20, 21, 23, and 24. 1976 

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Infrared and visual sighting 
DEPAITMENT OF TllNSPOITATION 

I.S. ClAST 'IU' .cuumPlIC .IIT 

lirhr .. 'dlltill Thr •••• 11I Pr'llI. 

SURFACE ISOTHERMS . °C 

FEBRUARY lD. 11. 12. 20. 21. 23. IIIKI 24. 1976 Wilmington 

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219 

New 

STREAM WEST WALL CROSSING AS INDICATED 

BY INFRARED AND VISUAL SIGHTINGS 

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DEPARTMENT OF TRUSPORTATIOM 

I,S, ClUT nm ImlmanlC .IIT 

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SURFACE ISOTHERMS . °C 

MARCH 11, 12, 14,23-25. 1976 Wilmington 

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INFRARED AND VISUAL SIGHTINGS 

/ I /;>/ 

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JUNE 8-10, 1976 Wilmington 

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80·W 

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75· 

223 

/ GULF STREAM WEST WALL CROSSING AS INDICATED BY 

INFRARED AND VISUAL SIGHTINGS 

400N 

25°N 
DEPARTMENT OF TRANSPORTATION 

I.S. ClAST ClAn ICEUUUPIIC .. IT 

lilhlll Idialin nll •••• tll P"lla. 

SURFACE ISOTHERMS . 0& 

JULY 20-22, 27-28, 1976 

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28 '. 

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alllht in near .hore UUI , 2 to 3 ft .. .ode,ate allleWher • . :1 to '\ ft. : lwell ES(; 

at .. to 8 ft .: aky , 1/10 to 8110. Cu. C •• 

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SEPTEMBER 14-17, 1976 

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DEPARTMENT OF TRANSPORTATION 

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Air"r .. h~ilti'. all.,.eler Pr'lra. 

SURFACE ISOTHERMS . °C 

OCTOBER 19-30, 1976 Wilmington 

Cape 

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. . ,'. . . ", . .... 

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New 

/ GULF STRtAM WEST WALL CROSSING AS iNDICATED -BY 

INFRARED AND VISUAL SIGHTINGS 

30· 

227 
DEPARTMEIIT OF TRANSPDRTA TlON 

IS tuST CUll ICEUIUAPlIC UIT 

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SURFACE ISOTHERMS· °C 

NOVEMBER 16. 17. 19. and 20. 1976 Wilmington 

22 

New 

STREAM WEST WALL CROSSING AS INDICATED BY 

.INFRAREo,AND VISUoiIL SIGHT~GS 

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SURFACE ISOTHERMS . °C 

DECEMBER 8, 9, 10, 14, 15, and 16, 1976 

New 

Wilmington 

Cape 

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,. - , , . , 

NOT FLOWN DUE TO " 

9 ADVERSEllINe'-IFYll!lRfms ) '-

""'-·"' ''~'-''''''- '' '''' - ---~. • 

9 PERATI ON AL DIFFICULTIES 

I 

I 

229 

I GULF STREAM WEST WALL CROSSING AS INDICATED 

BY INFRARED AND VISUAL SIGHTINGS. 

30· 
Paper 14 

WATER COLUMN THERMAL STRUCTU~E ACROSS THE SHELF 

AND SLOPE SOUTHEAST OF SANDY HOOK, NEW JERSEY, IN 1976 

Steven K. Cookl 

INTRODUCTION 

In midyear of 1970 a cooperative ship of opportunity <SOOP) 

program was initiated between the National Marine Fisheries 

Service (NMFS) and the Maritime Administration of the u.S. 

Department of Commerce. The program, conducted in support of the 

Marine Resources Monitoring, Assessment, and Prediction Program 

of NMFS, involved the use of cadets from the U.S. Merchant Marinp 

Academy, Kings Point, NY, to collect expendable bathythermograph 

(XBT) data an board merchant ships operating along the east and 

gulf coasts of the United States. Since 1970 the SOOP program 

has expanded to include U.S. Coast Guard cutters and university 

research vessels in addition to merchant ships. 

The objective of this cooperative program was to identify and 

describe seasonal and year to year variations of temperature and 

circulation in the major current regimes of the western tropical 

Atlantic, Caribbean Sea, Gulf of Mexico, and western North 

Atlantic, utilizing the various ships as inexpensive platforms 

for the collection of data. 

Ships' routes were selected to obtain regular sampling in the 

most dynamically active areas of the Gulf of Mexico and the 

western North Atlantic. The features of principal interest were 

the Yucatan turrent, Loop Current, Florida Current, Gulf Stream, 

Shelf Water/SLope Water front, and a cold-water cell in the 

Middle Atlantic Bight. 

Because 1976 was such an anomalous year both in meteorology and 

oceanography in the Middle Atl?ntic Bight, a subset of the 1976 

SOOP data, co~prising 18 transects and one surface transect, was 

analyzed. 

lA tlantic Environmental Group, National Marine Fisheries 

Service, NOAA, Narragansett, RI ~2882. 

231 
The anoxic event which began early in the year off New Jersey and 

lasted through the srring and summ r of 1976 necessitated a 

detailed analysis of the thermal water colu~n structure , 

considering how it evolved, was maintained, and eventually 

declined. Oxygen depletion in the bottom waters over a large 

area off the coast during the ummer had sev re effects on the 

sport and commercial fisheries. The immediate impact included 

finfish and shellfish mortalities and unusual fish distribution 

patterns ana concentrations. Likely causes of the oxygen 

de~letion can ~e traced back to anomaLous environ ental 

conditions in January and February of 1976 in the ~iddle tLantic 

Bi']ht (A rmst rona, Parer 17)_ 

HISTORICAL SU .'1ARY 

~ater te~peratures in the ~iddLe Atlantic ;9 t range from a 

minimum of <3C in the New York Biq t in F ruary to >27C off Cape 

Hatteras in August (Bumpus et al. 1973 T e annual range of 

surface tempe rature may be >15C in the SLope ater to >20C in the 

Shel f water. 

Minimum winter temperatures are reached in late February or earLy 

~arch and may be as low as 1C. Dur;no this coldest season the 

Shelf Water column is well mixeo (isot ermal) fro surface to 

bottom and extends out to the Shelf Water/Slo e Water fron (a 

aoproximately the 1G O-m isobat) (Gunn, Pa er 18). Irregular 

warming usually be9ins in late February or early arch, and -

thermocline develops in Late A ril or early ~ay. 

A rather intense thermocLine develops dur;nr. the sum er, sealinc 

off the bottom waters and isolating a pooL or celL of cold winter 

water that rests on the bottom surrounded shoreward, seaward, an 

~bove by warmer water. As the su~mer progresses into earLy falL, 

this cold cell tends to erode in extent and increase i 

temperature. This erosion is presumably caused by mixing fro 

above with warmer near surface waters and from a "calving" 

process, described by Whitco~b (1~70), ~here ~arceLs of this 

cooler water break off and flow and mix seaward into the Slope 

water. 

For this report all figures have ~een annotated to show: 

SheLf Water/Slope Water front 

Shelf ~ater/Slope Water meander 

North loJall of the Gulf Stream 

Anticyclonic warm core eddy 

Gulf Stream meander 

Flow d ire c t ion 

232 

- SSF 

- SSFM 

- GS 

- ACE 

- GSM 

- 9 into the page 

- 0 out of the page 
TRANSECT ANALYSIS 

Locations of features are given in ~arentheses in kilometers from 

the 200-m isobath. positive is seaward. 

Jgo~~rt. Unfortunately, the three January transects occurred in 

the latter part of the month, but still they are relevant in that 

they show the early beginning of the stratification which usually 

occurs in late February or early March. 

The ~QC~~£ Ril~i 76-01 (Fig. 14.1) crossed through the area 

during 24-25 January. This transect showed the normal isothermal 

water inshore with sLight warming of surface waters offshore. 

The sea surface temperatures (SST's) ranged from <4C to >21C 

which were warmer than usual (on the inshore end of the transect) 

for t~at tine of year. The Shelf Water/Slope Water front was 

crossed at station 3 (-65 km) and the north wall of the Gulf 

Stream was crossed between stations 4 and 5 (+160 km). 

The USCGC Qgilg~ 76-01 (Fig. 14.2) crossed through the area 

during 26-27 - January (just after the r:1Q!:!!!§£ Big~l). The ~§!.!.g~ 

section did not extend as far offshore as did the Biggi section, 

and therefore the SST's shown range only from <4C to >15C. Again 

the normal isothermal water structure was evident with a slight 

warming of the surface waters showing up, especially between 

stations 5 and 10 (-5J km to +75 km). The Sh e lf Water/Slope 

water front was crossed hetween stations 6 an d 7 (-15 km). 

The b~~h A!iga!ifQ 76-01 (Fig. 14.3) crossed through the area 

during 31 January-1 February. The SST's ranged from <5C to >14C. 

The nearshore water column structure was isothermal, while the 

offshore waters were beginning to show stratification. The 

subsurface warming (100 m) was probably due to Slope Water 

intruding up onto the shelf. The Shelf Water/Slope Water front 

was crossed between stations 12 and 13 (+15 km). 

While it may not have been obvious from these three vertical 

sections, comparisons with the past eiqht years of Gulf Stream 

SST data 2 indicated that the January surface water temperatures 

were about 0.5C wormer than normal and that some evidence, at 

least in offshore waters, showed that surface stratification was 

be~inning to develop early. 

2 

!.h~ Gulf ~!r:~~!!! [1Qo!bil ' ~\:U!lm~r:l' u.S. Naval Oceanographic 

Office, Vols. 4 through 9 (1969-1974); g~if~tr:~~~' NationaL 

Weather Service, Vols. I and II (1975-1976). 

233 
f~QrY~!~. The USCGC Bibb 76-02 (Fig. 14.4) crossed through th

area on 6 February. Th;-SST's had increased, and ranged from <7C 

to >14C. Stratification had definitely set in over the shelf

with verticaL temperature gradients as large as 0.4C/m at the 

thermocline. Patches of isothermal Nater extending to >100 

depth ~ere still evident offshore. The Shelf Water/Slope Wate

front was cro£sed between stations 2 and 3 (+15 km). 

The £~gqr! Q~1~Qg~! 76-02 (Fig. 14.5) crossed through the area 

during 7-8 February. The SST's ranged from <3C to 16C. This ~as 

a rather complex section showing some return of cooling and som

stretific ation. This on again off again cooling and warming 

not uncommon for this area at this time of year. These per

turbations in warming and cooling are probably caused by small

scale, short-lived forcing events, such as rapid frontal passing

and reversals in wind direction that affect shallow coastaL 

waters in a very complex fashion. 

The Shelf Water/Slope Water front was crossed between stations 1

and 14 (+45 km) with a smalL neander (also visible in sateLlite 

imagery) in the front between stations 9 and 14 (-170 km to 

+45 km). The north walL of the GuLf Stream was crossed between 

stations 15 aDd 16. 

The USCGC §~i12!iD 76-02 

during 27-28 February. 

temperatures and salinity 

couLd stilL determine the 

front (between stations 7 

«Be to >10C). 

(Fig. 14.6) crossed through the area 

Unfortunately only surface values o

were obtained, but from these data w

position of the Shelf ~ater/Slope Wate

and b, -10 km) and an increase in SST'

bgr£h. The ~Qrmg£ Rig~i 76-03 (Fig. 14.7) crossed through th 

area on 23 March. The SST's ranged from <7C to >19C 

Stratification of the water column was well established, wit 

surface to bottom temperature differences as large as 4C in <50 

depth. The Shelf Water/Slope Water front was crossed betweer 

stations 5 and 6 (-30 km). 

8~rii· The £lQQrt Q~f~Qg~r 76-04 (Fig. 14.8) crossed through the 

area during 3-4 ApriL. The SST's offshore had increased to >22C

The nearshore waters had warmed to greater than 7C, however, thE 

stratification appeared weak in this transect. The Shel1 

Water/SLope Water front was crossed between stations 11 and 1~ 

(+350 km). The north ~all of the Gulf Stream was crossed betweer 

stations 16 and 19 (+640 km) Nith a GuLf Stream meander occurrinc 

oetween stations 13 and 16 (+42C km to +5CO km). The distance; 

indicated are so great because the ship's track ran paralleL tc 

and just offshore of the 200 n isobath. Subtracting about 330 k~ 

would give more reasonable distances. 

234 
The bg~h A!igo!i£Q 76-04 (Fig. 14.9) crossed through the area 

during 24-25 A~ril. The SST's ranged from >11C to 19C. This 

rather complex section showed a large cold cell of 7C water 

overlying a warm cell of >10C water (obviously of Slope Water 

origin) between stations 3 and 12 (-350 km to -85 km). The 

cell-like structure of the warm water was probably an artifact of 

the contouring in that the transect was run 2t an oblique angle 

to the Shelf Water/Slope Water front rather than perpendicularly. 

Thermal stratification (gradients up to 0.1C/m) WdS evident above 

the cold cell (upper 30 m). This section was further complicated 

by the presence of two Gulf Stream meanders (verified by 

satellite imagery) occurring between stations 16 and 18 (+45 km 

to +160 km) and 19 and 21 (+195 km to +280 km). The finaL 

crossing of the north wall must have occurred to the east of the 

end of this tcansect. 

~gt. The ~Qrm~£ Rig~l 76-05 (Fig. 14.10) crossed through the 

area during 15-16 May. The SST's ranged from 11C to >19C in the 

Middle Atlantic Bight and increased to >25C south of Cape 

Hatteras. The cold cell consisted of mUltiple bubblelike 

structures that are probably an artifact of the contouring 

because of the highly oblique angle at which the cold cell was 

crossed on this transect. The SheLf water/Slope Water front was 

crossed between · stations 12 and 14, in about 50 m. A sharp 

thermal front occurred between stations 12 and 13 and a less 

sharp salinity front occurred between stations 13 and 14. 

The ~~1£~~[~ ~l 76-05 (Fig. 14.11) crossed through the area 

during 17-24 May. The SST's ranged from slightly >12C to a 

little <14C across the whole section. The cold cell extended out 

to the shelf break and its minimum temperatures were <8C. The 

stratification was normal for that time of year with surface to 

thermocline differences as large as 4C in <100 m depth. The 

Shelf Water/Slope Water front was weak but discernible between 

s tat ion s 5 and 8 ( + 30 k nI ) • 

J~o~. The ~~l~~~r~ II 76-06 crossed through the area during 9-13 

June. The SST's ranged from about 16C to 19C. The cold celL haa 

moved shoreward to about the 7S-m isobath with minimum temperatures still <8C. The Shelf Water/Slope Water front showed up 

between stations 5 and 6 (+20 km) as a weak subsurface thermal 

front. Stratification was fairly intense with surface to bottom 

temperature differences as large as 1QC in <50 m depth. 

J~l~. The ~Qtmg~ ~ig~i 76-05 (Fig. 14.13) crossed through the 

area during 6-7 July. The SST's had increased, and ranged fro~ 

22C to >27C. The cold cell was generally <8C and extenaed off 

the shelf break. The Shelf Hater/Slope Water front apparently 

W3S crossed near station 41 ~-95 km), well seaward of the 1~C-rr 

isobath. Its location was uncertain, because no thermal 

structure was ~resent to identify the front and it was 

235 
arbitrarily located at the 34.5 0/00 su rface isohaline. Th

stratification was intense, with surface to bottom temperature 

differences as large as 14C in <50 m depth and gradients >0.5C / 

at the thermocline. The north wall of the Gu lf Stream wa

crossed betweeen stations 36 and 37 (+240 km). 

a~gY~l. There was no SOOP transect during this month 

Middle AtLantic Bight. 

in the 

~gQlg~Qgr. The ~Qrm2£ Riggi 76-09 crossed through the area 

during 1-2 Se~tember. The SST's had reached their peak and 

rangea from 2JC to 2bC. The coLd celL was stilL well deveLope

but had warmed; the voLume of water <hC was much smalLer than in 

JuLy. The Shelf Water/Slope Hater front was sligh ly sea ward o

the 200-m isobath (+5 km) and had a weak surface temperature 

signal. The 34.50/00 surface isohaline was a ain used to 

identify the front. The stratification was still strong with 

surface to bottom temperature difference~ as large as 10C in 

<50-m depth. The nort~ waLL of the GuLf Stream was crossed 

between stations 12 and 13 (+24) km). 

Q£lQQ~r. The h§~h Iyrkitg 76-10 (Fig. 14.15) crossed through the 

area during 7-8 October. The SST's ranged from <17C to >23C

The cold ceLL had a double bubbLe shape with the minimum 

temperature «12C) occurring within the shoreward bubbLe and the 

war~er temperature «13C) occurrin9 within the seaward bubbLe

The SheLf ~ater/Slope water front was crossea at station 

(-300 km) and possibLy again between stations 1C and 1

(-100 km). A GuLf Strean meander occurred at station 2

(+210 km) with the other haLf of the meanaer occurring just t 

the east of station 22 (+310 km). 

The USCGC §§ii§!io 76-10 (Fig. 14.16) crossed through the are 

ouring 23-24 October. The SST's ranged fro~ 14C to 20C . Th 

cold ceLL was quite eroded and had a double bubble shape agai

with the shoreward bubbLe again having the Lower temperatures 

below 11C on one station and ~enerally <12C. The seaward bubbLE 

was warmer, with minimum temperatures at least 1 deg higher thar 

those of the shoreward bubbLe. The SheLf water/SLope Wate r fron 

was crossed between stations 7 a~d ~ (-20 km) and was shoreware 

of the 100 m isobath. At this time of year the thermc.L structurE 

of the front was we~k, and it was identified mostly by thE 

34.5 0/00 isohaLine. stratification had weakened considerablYI 

and the faLL overturn was in prooress. 

~QyglliQgr· The b§~h I~rkitg 76-10 (Fig. 14.17) crossed throug 

the area during 17-18 November. The SST 's ranged from 11C t 

20C. The Shelf Water/Slope Water front was crossed betwee! 

stations 35 and 34 (-0 km), and had a weak thermaL signature. A

anticyclonic eddy was crossed between stations 26 and 23 (+310 k 

to +420 ~m) with the north walL of the Gulf Stream being to th 

236 
east of the end of the transect. The fall overturn had mixed 

away all thermal stratification over the shelf. The water column 

was nearly isothermal, ranging from 11C on the shelf to 14C just 

off the shelf. 

~~f~mQ~r. The USCGC ~iQQ 76-11 (Fig. 14.18) crossed through the 

area during 4-5 December. The SST's ranged from <9C to >20C. 

The cold ceLL had eroded away with the overturn and the Shelf 

Waters were isothermaL, ranging from 10C on the inner shelf to 

12C on the outer sheLf. The Shelf Water/Slope water front was 

evident between stations 2Y and 28 (+55 km) with a fairly strong 

thermal front. The north wall of the GuLf Stream was crossed at 

station 15 (+450 km). This distance is overly large because the 

transect paralleled the continental shelf. 

The USCGC §211~!iD 76-12 (Fig. 14.19) crossed through the area on 

21 December. The SST's ranged from >7C to <16C. The SheLf 

Waters were isothermaL, ranging from 9C to 11C (onshore to 

offshore). The SheLf Water/Slope Water front was crossed between 

I stations 4 and 5 (-1G km), and had a strong thermaL signature. 

SUMMARY 

Water temperatures in the Middle Atlantic Bight in 1976 generall y 

foLlowed narnaL trends for most of the year. However, two 

anomalous conditions arose during Late winter an d early spring. 

During Late winter the SST's averaged about D.SC warmer than 

usual. During spring the nearshore surface salinities were 

greatLy reduced. Sometimes th~se reduced surface saLinities 

extended beyond the SheLf Water/Slope ~ater front with values of 

<28 0/00. 

A combination of the high river discharge in spring coupLed with 

slightly increased surface temperatures Led to earlier than usuaL 

stratification in the nearshore zone. 

The offshore waters (at the sheLf break and beyond) fol lowed the 

nQrmaL trends of warming and cooling in both intensity and 

dur?tion. Even the passage of hurricane Belle did little to 

interrupt the normal seasonal warming. 

237 
LITERATURE CITED 

BUMPUS, D. F., R. E. LYNDE, and D. M. SHAW. 

1973. Phy&ical oceanography. lrr S. P. Saila (coordinator), 

Coastal and offshore environmpntal inventory, Cape Hatteras 

to Nantucket Shoals, p. 1-1--1-72. Univ. R.I. Mar. Publ. 

Sere 2. 

WHITCOMB, V. L. 

1970. Oceanography of the mid-Atlantic Bight in support of 

ICNAF, September-December 1967. U. s . Coast Guard Oceanogr . 

Rep. CG 373-35, 157 p. 

238 
OlSTANCE (N. M1LESI-+ 

~5 

O. 60. 120. 180. 240. 300. 360. 

PARAMETER AT SURFACE 

D 

.L • 21 

10 12 11~ 16 18 20 

50 ' .0 

t,,, ,. 5.0 •. 0: ' .0 • l. 

I • r "1 · 1 I • 

O. 60. : 120. • 180.· 240. 300. 

I 

360. 

• • · • 

• • 

SSF GS 

• ® • • • • 0 

21 

50 

100 

150 

200 

250 

o. 60. 120. 180. 240. 300. 360. 

NORMAC R1GEL 7601 (500571 STAT10NS 1-9 

37. 

36. 

35. 

34. 

33. 

32. 

420. 480. 540. 

20 

l. 50 

r I 

420. 480. 540. 

. 0 

50 

100 

20 

150 

200 

420. 480. 540. 

1/24 76 - 1/25/76 

239 

0 

0 

"-

0 

~ 

tz 

....J 

a: 

CIl 

C) 

00 10 60 

so 50 

00 

30 

00 10 50 

CRU1SE TRACK PLOT 

Figure 1 4.I.-Horuontal di trihutioD of 

surfact> temPE'ratur (dt'gT , C) and 

surface salinit \ r _) and \ erti 1 di tnbu-

,,- JanUlH) 19; . 

( ) in th upper 

R I;· I, !4-
u 16 

(;) 

w 14 Cl 

w 12 a:: 

::> 

..... 

a: 10 a:: 

w 

0... B 2: 

W 

..... 

lIE 6 

4 

O. 

o 

en 

a:: 

w 

.... 

w 

~ 50 

:J: 

.... 

0... 

W 

Cl 

... 

100 

O. 

0 

100 

en 

a:: 

w 200 ..... 

w 

~ 

:J: 300 ..... 

0... 

W 

Cl 

... 400 

500 

600 

700 

BOO 

O. 

20. 40. 

PARAMETER AT 

20. 40. 

I] I STANCE (N. M I LESJ+ 

60. 

SURFACE 

60. 

BO. 

• • • SSF 

100. 120. 140. 

! = 

= 

~"f • ----".f 

~::: 

'::-10~~~· 

~ .. 

BO. 100. 120. 140. 

36. 

35. 

34. 

33. 

32 . 

31. 

160. 

0 

100 

200 

300 

400 

500 

600 

700 

160. 

DALLAS 7601 (50062 ) STATIONS 1-11 1/26/76 - 1/27/76 

240 

0 

0 

...... 

0 

~ 

.... 

z 

...J 

a: 

en 

(!) 

110 70 

110 70 

CRUISE TRACK PLOT 

Figure 14.2.-Horizontal distribution of 

sea surface temperature (degrees C) 

and sea surface salinity (%.) and vertical distribution of temperature (degrees 

C) in the upper 100 and 800 m; USCGC 

Dallas 76-01, 26-27 January 1976. 
DISTANCE (N. HILES ) " 

5 34. 

0 

0 

2 "-

33. 0 

>-

z 

32. -' 

a: 

U1 

(') 

31. 

O. 40 . BO . 120. 160. 200. 240 . 2BO. 

PARAMETER AT SURFACE 

~ 00 70 .0 

0 50 SO 

0 50 

00 100 

50 150 

~OO 200 00 00 

00 7. •• 

O. 40. BO. 120. 160. 200. 24~. 280. I 

I 

I CRU ISE TRACK PLOT I 

. I 

SSF 

0 

100 100 

200 200 

12 

00 10 300 

~OO 8 400 

00 500 

600 600 

700 700 

BOO BOO 

O. 40. BO. 120. 160. 200. 240. 280. 

LASH ATLANTICO 7601 (5006 4) STATIONS 1-13 1/ 31176 - 211176 

igure 14.3.-Horizontal distribution of sea surface temperature (degrees C) and sea surface salinity ("/_) and vertical distribution of temperature (degrees C) in the upper 200 and 800 m; La8h Atlantica 76-01, 31 January-I February 1976. 

241 
STATION NO. 

2 3 4 5 6 7 8 9 

16 36 

14 34 • 

(J) • 1> 

U 12 32 r 

0 

z a.: 10 30 - ~ --i 

W ~ 

8 28 

I- ~ I 0 

0 

6 I I.-SSF 26 

4 24 

41°00' 41°00' 

I • 

• 

400 00'N • 400 00'N 

• ~ 

• O~ ,0 

0 • 

SSF / 

• 

39°00' 39°00' 

·9 

74°00'W 72°00' 

USCGC GALLATIN 76-02 

Figure 14.6.-Horizontal distribution of sea surface temperature (degrees C) and sea surface salinity (%.); USCGC 

Gallatin 76-02, 27-28 February 1976. 

244 
24 

20 

16 

12 

B 

4 

o 

50 

100 

150 

200 

o 

100 

200 

300 

400 

500 

600 

700 

BOO 

DISTANCE (N. HILES)+ 

-, ____________________________________________ ~37. 

36. 

35. 

34. 

33. 

32. 

-r--~~,_----_r-L--_,------,_----_.------,_----_+3). 

o. 

O. 

40. Bo. 120. 160 . 200 . 240. 

PARAMETER AT SURFACE 

40. BO .• · 

· · · 

SSF · 

• 

· 

120. 160. 200. 240. 

~ 

14 •.• 

... 

~12~ ~::: ~10 

~8~"\\~:: ~ ~~ .. 

~6 ~:: 

12 

2Bo. 

2BO. 

100 

200 

300 

400 

500 

~ 600 

700 

-t~~~~~~~~~~~-------r------.------,-------+-BOO 

O. 40. BO. 120. 160. 200. 240. 2BO. 

o 

o 

"-

o 

z 

MORMAC R I GEL 7603 (50299) STAT IONS 1 - 15 3/23 /76 - 3/23/7 6 

245 

10 

50 50 

~o 

]0 

110 10 

CRUISE TRACK PLOT 

Figure ) .'.-Horizontal dl tnbution of sea urface temper lur 

(degree CJ and l"8 urI ce linih 

(' _) and H'rtil'lll dl tnbutlon of 

temperature (d ) ID the upper :?OO and 00 m; \Jormac RIG I 

.6-03, :!3 March 1 j • 
DISTANCE (N. MILES)+ 

u 24 ~37. t.:l 36. 0 

w 20 0 

0 .. ,. L3S. n w 

a:: 

:::J 16 ,.... 

I1- 3 Ia: 

a:: 12 z w 

a... I-33. E a: w on I-

)I( 

B t- 32. C) 

4 31. 

O. 60. 120. 1BO. 240. 300. %0. 2C. BO. 

PARAMETER AT SURFACE 

. " . ~ . . ~ = :: ::: :: ::: :: :. . :: :: :: 00 10 00 

0 0 50 

50 <;0 Vl 

a:: 

w 

IW C E 100 lOG 

I 

Ia... 7 w 

0 

150 .... :50 

8 

200 It . 0 200 )0 

• · 00 10 

O. 60. 120. IBO. 240. : 300·. 360. 20. BO. 

• • • . • • 

• • CRuISE RAC>' PL T 

SSF · GSM : GS 

~ 0) 0 

· • . ~ • ~ ... . " . ~ . . ~ ::: :. -. - :: :: ~ 

0 0 

100 f- 100 

Vl 

a:: 

w 200 I- t-- 200 W 

E 

I 300 ~ 300 Ia... 

w 

0 

.... 400 400 

500 500 

500 500 

700 700 

Figure 14.8.-Horizontal distribution BOO 0 

BOO sea surface temperature (degrees C) an 

O. 50. 120. lBO. 24 0 . 300. 350. 420. 4BO. sea surface salinity (,/_) and vertical distri

bution of temperature (degrees C) in thl 

EXPORT DEFENDER 750 4 (50713) STATIONS 1 - 22 4 / 3175 - 414175 upper 200 and 800 m; Export Defender 7 

04, 3-4 April 1976. 

246 
DISTANCE IN. MILES)" 

21 37. 

36. D 

18 D 

35. " D 

15 34. >-

>-

12 33. z 

...J 

32. a: 

9 en 

31. (!) 

6 30. 

O. 60. 120. 180. 240. 300. 360. 420. 480. 

PARAMETER AT SURFACE 

. " . . ~ ~ ~ ~ ~ ~ 00 10 00 

0 0 so 

50 SO 

00 100 

150 150 

200 200 

. 00 

O. . 60. 120. 180. 240. 360. 420. . 480 . 

SS r GSM GSM CRUISE TRACK PLOT 

· ~ 0181 0 

. · . " . . 0 0 ::: . ~ : ~ :: 

0 0\ v,~ , 

100 100 

.;;: 

200 200 

300 300 

:::. 

400 400 

500 .,: ~}" :.:~ .:::: . 500 

600 600 

700 ~ 700 

-.:; 

BOO 800 

O. 60. 120. 180. 240. 300. 360. 420. 4BO. 

LASH ATLRNT lCO 7604150712) STRT IONS - 22 4/24/76 - 4/25/76 

igure 14.9.-Horizontai distribution of sea surface tempt'rature (degrees C) and sea surface salirut} ("_l and \ertical di~lributlon oflemper • 

ture (degrees C) in the upper 200 and 800 m; Lash Atlantico 76-04. 24-25 prii 19;6. 

247 

<a 

•• 
u 

t:> 

w 

0 

w 

a: 

:::> 

...... 

ex: 

a: 

w 

0.. 

L 

w 

...... 

lIE 

en 

a: 

w 

...... 

w 

x: 

:r 

...... 

0.. 

W 

0 

'" 

27 

24 

21 

18 

15 

12 

9 

D. 

I) 

I 

I. 

I . 

50 

100 

O. 

DISTRNCE (N. HILESH 

70. 140. 210. 

PRRRHETER RT SURFRCE 

_N--'''''''.'''._~ 

70. 140. 210. 

280. 

SSF 

280. 

350. 420. 490. 

"".,.._.O_Nft _____ NN"" ... 

350. 420. 490. 

37. 

36. 0 

0 

"-

35. 0 

>-

34. ...... 

z 

33. -' 

ex: 

en 

32. (') 

31. 

560. 

50 

560. 

MORMRC RIGEL 7605(50822) STRTIONS 001 - 024 05/15/76 - 05/16/76 

80 70 

so 

~o 

30 

80 70 

CRU I SE TRACK PL 

I iR'urc 11.10. Horizontal distribution of sea surface temperature (degrees C) and sea surface salinity (%.) and vertical distribution of tern· 

perature (degrees C) in the upper 100 m; Mormac Rigel 76-05. 15-16 May 1976. 

248 
14 

13 

12 

II 

0 

25 

50 

75 

100 

0 

50 

~ 100 

u 

u 

E 150 

t: 

200 I... 

U 

D 

250 

300 

350 

/' 

/' 

O. 10. 20. 30. 40. 50. 60. 70. 80. 90. 100. 110. 

DI~TANCE (N. M. ) 

2 3 4 5 6 7 8 9 

O. 10. 20. 30. 40. 50. 60. 70. 80. 90. 100. 110. 

SSF 

2 3 4 5 6 7 8 9 

O. 10. 20. 30. 40. 50. 60. 70. 80. 90. 10Q 110. 

DELAWARE II 76-05 STATI ONS 1-9 5/17/ 76 

249 

34. 

0 

0 ~ 

>-

f--

z 

-.J 

<l: 

(f) 

~ 

29. 

a 

25 

75 72 

50 40 1----1lI1...----.:: ......... -------1 4 0 

75 

75 72 

CRUISE TR A CK PLOT 

Figure 14.11.-Horizontal distribution of sea surface temperature (degrees C) and sea surface salinity 

(,/_) and vertical distribution of 

temperature (degrees C) in the upper 100 and 350 m; Delaware II 

76-05, 17-24 ~fay 1976. 

5 / 24 / 76 
<3 

(!) 

w 

0 

w 

a:: 

~ 

t-

<I: 

a:: 

w 

0... 

~ 

W 

t-

'" 

(f) 

a:: 

w 

tW 

~ 

I 

to... 

W 

0 

(f) 

' a:: 

w 

tW 

~ 

I 

to... 

W 

19 

18. 

17. 

16 

0 

25 

50 

75 

100 

o 

100. 

o 200 

300 

34 

0 0 

~ 

r 32 tZ 

....J 

<I: 30 (f) 

, 

28 

0 10. 20 30 40 50 60 70 80 90 100 110 120 

DISTANCE (N M) 

2 3 4 5 6 7 8 

0 

25 

50 

13 

75 

100 

o 10 20. 30 40 50 60 70 80 90 100 110 120 

2 3 4 5 SSF 6 7 8 

o 

100 

12-----

200 

--

O. 10. 20. 30. 40. 50 60. 70. 80. 90 100. 110 120. 

DELAWARE n 76 - 06 STATIONS 1-8 6/9/76 - 6/13176 

250 

'·30' 

O· 4 

74·30' 7 ' · 3C' 

CRUISE TRACK PLOT 

Figure 14.12.-Horizontal distribution 0 

sea surface temperature (degrees C) and 

sea surface salinity (,/_) and vertical distri' 

bution of temperature (degrees C) in the 

upper 100 and 300 m; Delaware II 76-06, !J, 

13 June 1976. 
DISTANCE (N. HILES1 + 

28 37. 

0 36. 0 27 

"-

26 35. 0 

>-

25 34 . z 

24 33. ~ 

a: 

r.n 

23 32. (!J 

22 3l. 

O. 50. 100. 150. 200. 250. 300. 350. 400. 450 . 

PARAHETER AT SURFACE 

80 70 60 

o 50 50 

50 50 

100 100 

00 

20 (0 .. 150 ISO 

19 

200 200 30 ~---- 30 

80 70 60 

O. 50. 100. 150. 2Qo. 250. 300. 350. 4 00. 450. 

SSF GS CRUISE TRACK PLOT 

® 

• ; ~ ; ; = ~ " ~ :: ~ ~ .- :II: :: ::: ;; ~ ~ ~ ~ ~ ::l 

0 0 

100 100 

200 

~200 300 300 

400 ~ 400 

500 500 

600 600 

700 700 

Figure U.13.-Horizontal di Iribution of sea surface temperature (de800 800 gree-s Cl and 'ea ur(a e , hmt) 

("/_) and \erticaJ di tribution o(ternO. 50. 100. 150. 200. 250. 300. 350. 400. 450. perature (degr C) in the upper 

200 and 00 m; ~formn c Rilt I j 

MRHA C RIGEL 7605 (50 822 ; STATIO NS 0 48 - 025 07,07,76 - 07106176 6-7 Jul\ 1976. 

251 
u 

t.:) 

w 

28 

o 26 

w 

a::: 

=> 

~ 24 a::: 

w 

0.... 

:E: 

w 22 t-

)I( 

LJ') 

a::: 

w 

t-

:r: 

to.... 

W 

o 

20 

o 

50 

<I> 150 

200 

O. 

O. 

DISTANCE /N. MILES)';' 

- - '<"\ 

50. 100. 150. 

PARAMETER AT SURFACE 

50. 150. 

SSF 

r 

200. 

,. 

. 

r 

250. 

! :: :: 

20C. : 250. . 

GS 

o 

30e. o. 

.. . 

'10') 

F

38 . 

37. 

35. 

o 

100 

150 

200 

o ----,- 0 

100 100 

LJ') 

a::: 

~ 200 ~ 

:r: 300 to.... 

W 

o 

<I> 400 

500 

600 

700 

800 

O. 50. 100. 

200 _____ ~. D 

300 

~'D 400 

500 , D 

600 

700 ~ •. o 

150. 200. 250. 300. 350. 400. 

(') 

..., 

,.. 

... 

/ 

M~RMAC R'GEL 7609/50867) STATI~NS 001 - 019 09/0 1/76 - 09/02/76 

252 

o 

70 

p , 

Figure 14.14.-Horizontal distrib 

tion of sea surface temperature ( 

grees C) and sea surface salini 

("/_) and vertical distribution 

temperature (degrees C) in the u 

per 200 and 800 m; Mormac R' 

76-09, 1-2 September 1976. 
Figure 14.15.-Horizonta1 distribution of sea surface temperature (degrees C) and sea surface salinity (%.) and vertical distribution of temperature (degrees C) in the upper 200 and 800 m; Lash Turkiye 76-10, 7-8 October 1976. 

253 
OISTRNCE (N . MILES ) + 

u 20 40. 

l:) 19 39. 0 w 0 0 38. "- 18 0 w 

cr: 37. ~ 17 >- .... 36 . .... a: 

cr: 16 z w 35. a.. -' x: 15 a: w 34. (J1 

(!) lIE 14 33. 

13 32. 

'J . 20 . 40. 60. 80. 100. 120. 140. 160. 180. 

PRRRMETER ,n SURFRCE 

110 70 

o so so 

(J1 

.... 

cr: 

w 

w ~ 

:r::: 50 50 

:x: .0 ~o 

.... 

a.. 

w 

0 

.. 

100 100 50 '0 110 70 

O. 20. 40. 60. ~. 100. 120. 140. 160. 180. 0 

0 

0 CRUISE TRRCK pun 0 

SSF 

~ ~ ! ~ ~ = ~ . 0 0 

18 19 

~o .• I . • V> : 00 ... cr: 100 ---.J' . O 

. 

W ~' .. w 

~:: ::r. 

"I: 

.... 20C 

~ .. 200 a.. ., w 

0 

~: .. ~OO 300 

~8 .. 

00 -J /\ .. 400 

~6 

Figure 14.16.-Horizontal distribu· 

SOD 500 tion of sea surface temperature (de· 

grees C) and sea surface salinity 

180. ("I.) and vertical distribution of 

Gil l llTIN 7610lS08361 S A NS 016 - temperature (df'grees C) in the up· 

01 10/24176 - 10/23176 per )00 and 500 m; USCGC Gallatin 

76·) 0, 23·24 October J 976. 

254 
22 

20 

18 

16 

I~ 

12 

10 

o 

50 

100 

ISO 

200 

o 

100 

200 

300 

• ~OO 

500 

600 

700 

BOO 

DISTANCE (N. HILES)" 

37. 

0 

0 

36. "-

0 

~ 

35. rz 

-' 

34. ex: 

en 

(!) 

33. 

O. ~O. 80. 120. 160. 200. 2~0. 280. 320. 

PARAHETER AT SURFACE 

It It ... It 

50 1 , . 

100 

1 , . 

ISO 

20 0 

• • O. ~O. 80. 120. 160. 200. 280: 320. 

• • • • • • • ,. • · SSF ACE 0) 

a It .. • It p ;; It 

0 ... "-12 

100 

200 

300 

~oo 

500 

600 

• 700 • • • • • • 800 

O. ~O. 80 . 120. 160. 200. 240. 280. 320. 

LASH TURKIYE 7610(50869) STATIONS 039 -023 11/17/76 - 11/18/76 

255 

50 

~o 

'0 

so 70 60 

50 

~o 

30 

60 70 60 

CRUISE TRACK PLOT 

Figure 14.17.-Horizontal distribution of sea surface temperature (degrees C) and sea surface salinity 

(%.) and vertical distri.bution of 

temperature (degrees C) in the upper 200 and 800 m; Lash Turkiye 

76-10, 17-18 November 1976. 
:::: 20 c... 

~ 16 ,;;) 

~ ~2 a: 

w 

~ a UJ 

... 

1: 

> 

(l. 

UJ 

) 

'*' 

c., 

2C(, 

1 

c. 

o -*-* 

(f) 

cr 

w 

..... 

w 

E 

10:: ~ 

;= 2CO (l. 

w 

o 

.\> 

300 

400 

10 

Iilo 

.:.: 

0: lRNCE . 

• II t 

I 

o 

I ' • 

1~ 

.. 

1./0 

60 

SSF 

:; 

*- -* I 

I ) 12~ 4;--? 116 \ 

.'~ 0 I :0 /" 

.: ..... 

~ -----"'--""'--

~--- .o/"_ 

~ 

12 

14 

12 

.. 

GS 

300 

00 

500 ~~~~~~~----~----,----,--__ ~~500 

o. 60. 120. 180. 240. 300. 360. 420 . 

8IBB 7611 (50892) STRTJONS 034 - 012 12/05176 - 12 /0 4176 

256 

FiK\ll"e 11.1 .-Horlzontal di tribution of ,ea .u.-faCt' tem~ratUTe (dt'-

gre<?' Cl and ea urial-e .almit, 

("1M 1 and, ertical di.tribution of temperature (degree_ Cl in the up~r 

:!OO and .')00 m: L'SCC Bibb 76-11. 

1-5 December 1976 
16 u 

'" UJ 14 0 

UJ 

a:: 

~ 12 Ia: 

a:: 

UJ 10 0... 

:!: 

UJ 

IlIE 

8 

6 

o 

(J") 

a:: 

UJ 

IUJ 

:!: 50 

I 

I0... 

UJ 

Cl 

.. 

100 

o 

'" 100 a:: 

UJ 

IUJ 

:!: 

I 

t- 200 o... 

UJ 

0 

... 

300 

400 

500 

O. 

DISTANCE (N. MILES)~ 

20. 40. 

PARAMETER AT SURFACE 

60. 80. 

• • • • • 

SSF 

100. 120. 

~'~~~~'."O~~~==~~~~~~~~L-~~L-~~--,-O JO.O •. 0 

100 

200 

300 

400 

O. 20. 40. 60. 80. 100. 120. 

GALLATIN 7612(50929) STATIONS 013 - 001 12/21176 - 12/21176 

257 

70 

50 50 

~o ~o 

30 30 

eo 70 

CRUISE TRACK PLOT 

Figure 14.19.-Horizontal distribution of sea surface temperature (degrees C) and vertical distribution of 

temperature (degrees C) in the upper 100 and 500 m; USCGC Gallatin 

76-12, 21 December 1976. 
Paper 15 

ANTICYCLONIC GULF STREAM EDDIES 

OFF LHE NORTHEASTERN U~ITED STATES DURING 1976 

David Mizenko and J. Lockwood Chamberlin l 

INTRODUCTIO~ 

This report continues for a third year (1976) an analysis of the 

movements of anticyclonic Gulf Stream eddies in the Slope ~ater 

region off Ne~ England and the Middle AtlBntic coasts. A report 

on these eddie.s during 1974 and 1975 was prepared by Bisagni. A 

general summary of information on the formation, structure, and 

dynamics of anticyclonic eddies is available in his report, and 

is not included here. 

The information provided here on the eddies is basically the same 

as that presented by Bisagni. 2 It aiffers in minor ways, as 

described in t .he following sections, because of some differences 

in our methudology and improvements in the primary information 

available from satellites. 

Some additional information is also given, especia lly on the 

formation and destruction of the individual eddies, the surface 

boundaries of the eddies, and a zonal ' analysis which summarizes 

information on the movements of the eddies relative to ~ne 

another. 

~~!hQQ~ Q1 ~O@l~~i~ 2DQ ~Q~f~~~ Q1 IDiQfID§!iQD QD ~gg~ ~~ri~~~ ~~~ili~Q~ ~Qg ~~~Qg~ti~~ 

The positions and surface boundaries of the eddies, during 1976 

(Figs. 15.1-15.7), were largely taken from Experimental Ocean 

Frontal Analysis charts issued weekly by the U.S. Naval 

Oceanographic Office. Additional information ~as obtained from 

infrared imagery from the NOAA GOES 1 and 2 satellites, enhanced 

lAtlantic Environmental Group, National Marine Fisheries 

Service, NOAA, Narra~ansett, RI 02882. 

2Sisagni, J. J. 1976. The passage of anticyclonic Gulf Strea 

eddies through Deepwater Dumpsite 106, 1974-1975. NOAA Du psite 

Evaluation Report 76-1, 39 P. 

259 
Pape r 15 

for s e a s ur f ac e te mpe rature (abo ut 6 to 8 images available per 

day), a nd the er iment al Gulf Stre ~ Analy s is, issued weekly by 

the National Env iron menta l Satellite Service. For the special 

analysis of the Fe bruary-April period , NOAA-4 satellite imagery 

was also used. 

Positions based on imagery that clear l y shows the surface 

boundaries of the e ddies are drawn with so l id lines; uncertain 

positions from unclea r imagery are drawn with d ashed lines. The 

dots (Fi g s. 15.1-15.7) are the centers of t he ed d ies as estimated 

by eye from tne surface boundari~s. Surface bound a r ies are only 

s ho wn for representative states in the lifeti me s of the eddies. 

8 0th the positions and boundaries should be reg arded as rough 

approximations, because the surface expressions o f the eddies in 

t he imagery are often distortions of the subsurf ace structure. 3 

Po toc s ky (1976) has pointed out that eddi e s entraining Shelf 

Wa ter may ap~~ar much smaller in satellit e imagery than is 

ind icated by the subsurface structure, and t ha t th is distortion 

;s mos t frequent west of 70W. 

Eddie s that made surface contact with the Gulf Stream were still 

regar ded as eddies, so long as it appeared f ro m the imagery that 

thei r circulation was lar g ely se parate trom th at of the Stream. 

In t he Exper i mental Ocean Frontal AnaLysis , eddies which Later 

made such contact were LabeLed as meanders. 

whiLe the methods used here are basically si milar to those of 

Bisag ni (see footn o te 2 ), there are some impo rtant differences in 

d eta il. On his "trajectory" maps, Bisagni shows aLL positions, 

su re and estimated, from several sources . ~e have avoided 

p lotting estimated positions except where Long time gaps exist 

between sure positions, and have given on ly one position for an 

ed dy on any given date. 

Thoug h simiLar data sources were used, thei r quality has improved 

ma rk e dly since the period 1974-75 studie d by Bisagni. This is 

esre cially true of the ExperimentaL Oce an Frontal Analysis 

cha rts, which durin g 1974 lacked the de taiL, accuracy, and 

documentation ~hich has since been inc o rporated--especiaLly 

dur i ng 197b. This imrrovement has allowe d more accurate data to 

be pr esented here than was aV;:dlable to Bis a gni. 

The dates of eddy formation and destruc tion were interpolated 

whe n necessary. For example, if a feat ure was clearly a Gulf 

St ream meander on 15 October and an e ddy on 1 9 Octo ber, it is 

3Chamberlin, J. L. 1977. Monitori ng e ff e cts of Gulf . Stream 

me anders and warm core eddies on t he contin ental shelf and slope. 

Int. Comm. Northwest Atl. Fish . , Sel. Pc p . 2 : 145-153. 
ssumed to have detached from the Gulf Stream as an eddy on 

7 October. These interpolations are accurate to within a week 

r less. Bisagni used the dates an eddy was first sighted and 

last sighted as his formation and destruction dates, makin g his 

stimates of eddy lifetimes a little shorter (on the order of a 

week) than would be obtained by our method. Infrared imagery 

rom the Geostationary Orbiting Environmental Satellites at 3-h 

intervals, which 8isagni did not have available, was very useful 

for establishing such dates. 

0nly eddies that were observed west of 60w are considered in this 

report. These are labeled by the year in which they formed plus 

a sequentially assigned letter. The dates of their formation and 

destruction, and the numb~r of days they survived, are summarized 

in Tat-le 15.1. 

Table 15.1.--Summary of estimated eddy formation 

and destruction dates and days of survival. 

£~g:t ~~1~~ Q~:t~ 

75E 7/23/75 3/27/76 £":48 

751 11/1/75 3117/76 137 

76A 2/27176 3130/76 37 

768 4/1176 ? >98 

76C 4/19/76 - 10/15/76 179 

76 D 5/20176 2/4177 260 

76 E 5/28176 7/24/76 57 

76 F 10/15/76 214/77 11 2 

76G 10127/76 5113177 198 

Tot a l eddy-days in 1976: 

Date first observed (see text footnote 2). 

Subject to reV1Slon. 

May have survived into August. 

Totals by quarter: 

Jan-Mar 199 

Apr-Jun 236 

JuL-Sep 2CR 

Oct-Dec 249 

(See also 8isagni 197b). 

261 

Q~:t~ jo 

12ZQ 

87 

80 

32 

>90 

179 

225 

57 

77 

65 

>892 
Paper 15 

EDDY HISTORIES - 1 76 

T~o eddips survived 1975 into 1~76 5 Bno ~l). E 75 

(Fig. 15.1), first observed on 2.3 JJly 1975 {Sis (ni 's 

was off southern DeLaware with an pp"r n urfcc Ii m 

about 40 nm (70 km) t the st rt of 1~7. An 

bathythermograph <XBT) survey on 18 f.bruary and 1. r 

maximum Core temperature of 13C xt nding to n Rrly 3G~ 

(Cook et ale 1Y76). This eddy co L sce wi th -ulf 

about 27 March. 

Eddy 751 (Figa 15.2), which for ;n rLy 

not dpparent in s teLlite ima ry aft r the 

month for two months until the end of Januar 

Located at o6w with n opar nt surfac 

(170 km). After moving south.est about 1 nO nm 

vicinity of b3W, the eddy a pearcd to be l rg l 

1 75, 

of 

17 March, by encroachme~t of ~ Lf Stre meander 

and 15.oc). About 1 A riL, I-lart of t \;5 n a der p r 

detache from the Stream as anoth r e dy (76 ), i dicd ed 

extensive patch of Gulf Strea at r at 67 3~' on 

(fig. 15. e). Another ossi Le int rpr tion 0 t 

that eddy 751 was not d stroye durin and t 

and 751 are the same. 

i 

of a n 

to ha 

s 

7 f.pril 

An XBT section from _iQ_tCQaa i_ on 2-3 priL Line AS 

Fig. 15.9) in the area of the rlTi pate indicates nticyclonic 

circuLation, especialLy in th form of the isot ~r~s for 12C a d 

colder, but bee use of the section's Lac nt, do s not 

determine the feature as a meander or eod , ~Lt ouqh the thermal 

structure does show surface connection i h h Gulf ream. 

The very steep thermal radie t at the inshore largin of the eddy 

(Fiq. 15.9) is based on the trac s frolTi thr e XB pro s drooped 

near together in quick order. An additional XBT sec ion alan 

line BC in the inset map on Fig re 15.9 is n t re~r duce( in this 

report, but shows a similar steeD thermal ra ient (at 

position C). An eastward current c n e inferred on the offshore 

side of the gradient. 

The history of eddy 763 (Fig. 15.2) is not clearLy apparent In 

the satellite imagery. The 24 April Dosition ;s base on a ~armwater patch of uncertain character. The 29 ay position is ased 

on a protrusion of Shelf water that h2s the appearance of 

entrainment around an eddy with a surface diameter of about 5J nm 

(90 km). The presence of 13C water to a depth >155 m over the 

outer shelf south of New EngLand (71W12 1 ), in an X T section from 

the ~~~t~~rq on 11-12 May, pr8viced evidence of the passage of an 

eddy. If the deep 13C water was from this eddy, then 766 ~oved 

westward much more quickly than was indicated by satelLite 

imagery, and then remained in the area of 71~ for about three 

weeks. This eddy may have been the one that appeared in the area 

262 
of Deepwater oumpsite 106 (38N4J'-39NOO', 72WOO ' -72W30') at the 

end of June as shown by several X8T sections. · After May, 

however, the history of the eddy was not revealed in satellite 

imagery. 

Eddy 76A formed about 22 February from a large meander centered 

at 63W (Figs. 15.3, 15.8a, 15.gb). The large decrease in apparent surface diameter of this eddy fro~ 140 nm (260 km) at the end 

of February to 100 nm (190 km) at the end of March was probably a 

result of deceptive surface expression. A "hydrocast transect 

from the RV ~tQii ~~~£k~l made on 20 March (Fig. 15.10) showed 

this eddy to be a smoothly structured mass of Sargasso Water, 

with a sigma-t range of only 25.9 to 26.3 at stations 1 to 4 

(except in a few of the deepest samples at stations 2 and 4). 

A special set of diagrams (Fi9. 15.8) has been prepared to 

illustrate major interactions between the Gulf Stream and 

anticyclonic eddies in the area southeast of Georges Bank fro~ 

mid-February through April. Involved in these interactions were 

two large chaoges of course by the Stream and the destruction of 

eddies 751 and 76A, a5 well as the formation and destruction of a 

cyclonic eddy. 

On 17 February (Fig. 15.8a), eddy 751 lay south of Georges 

Bank, and a Gulf Stream meander was separating as eddy 76A. 

On 28 February (Fig. 15.bb), eddy 751 was entraining warm 

Gulf Stream water, and eddy 76A was fully formed and had 

moved westward. 

By 24 March (Fig. 15.8c), a developing Gulf Stream meander 

had encroached on eddy 751, apparently destroying it. Eddy 

76A moved westward and entrained warm Gulf Stream water. 

By 27 March (Fig. 15.8d), Sulf Stream water was 

from the meanaer south of Georges Bank as eddy 

76A ceased entraining Gulf Strea~ water and was 

losing water to the Gulf Stream. Meandering of 

intensified southeast of eddy 76A. 

separatin~ 

76B. ~ddy 

apparently 

the Strea~ 

By 7 April (Fig. 15.8e), eddy 76a had separate d from the 

stream south of Georges Bank and had moved westwaro. The 

Gulf Stream changed course throu~h the northern portion of 

eddy 76A, forming a broad meander that incorporated this 

eddy. T~e former path of the Stream to the south became a 

cyclonic eddy. A hydroc3st transect from the ~i~£lQQ made 

4 J • J. Sisagni, Atlantic Environmental Group, NMFS, Narragansett, RI 02882. Pers. commun. 

263 
Paper 15 

on 4-7 ApriL (Fig. 15.11; station location pLotted on 

Fig. 15.8e) showed only one crossing of the Gulf Stream 

axis, inJicdting that the GuLf Stream had assumed its 

directly eastward path by the time of the section. The rise 

in isoth~rms and isohalines at station 4 was due to the 

proximity of this station to the Gulf Stream's northern 

edge. 

On 14 April (Fig. 15.8f), eddy 768, south of Georges Bank, 

was not visible in satellite imagery. The Gulf Stream had 

merged with the west margin of the cyclonic eddy. 

By 18 ApriL (Fig. 15.8g), the cyclonic eddy was incorporated 

into the Gulf Stream, but the former path of the Stream was 

not completeLy abandoned. Hydrocast stations (Fig. 15.2, 

8e loqors~, 17-19 April) of le~ AB were entirely in Slope W~t~;~-~hile the middle stations of leg 8C were in the Gulf 

Stream, providing agreement with the surface pattern shown 

in Fi9ure 15.89. Because of the placement of stations, the 

link between the old and the new Gulf Stream paths was not 

recorded in Figure 15.12. 

On 24 ApriL (Fig. 15.8h), eddy 76C formed from the remnants 

of the oLd Gulf Stream path. 

The position of eddy 76C (Fig. 15.3), following its formation in 

April, was not cLearly seen in the satellite imagery until 

August. The position for 15 ~ay was based on a warm water patch, 

and for 28 July, a suggestive Shelf Water protrusion. The 

28 July position was especially questionable, because in order to 

reach its fdirly certain ~~sition of 18 August, the eddy would 

have had to travel at an aver3ge rate of at least 6 nm (11 km) 

per day. This speed is inconsistent with average rates of up to 

4 nm (7 km) per day that we have calcuLated for other eddies in 

1976. Evidence for the passage of this eddy south of New England 

was provided oy 13C water to a depth of >140 m over the outer 

continentaL &heLf at 71N10', in an XBT section from the Q£~2QY~ 

on 12-13 August. The satellite imagery provides no clear picture 

of this eddy's size until late August when the apparent surface 

diameter was 60 nm (110 km). The surface expression shrank 

markedly during late September and October, and the eddy 

coaLesced with the Gulf Stream about 15 October. 

Eddy 76D (Fiq. 15.4) formed about 20 ~ay from a large meander 

centered at 65W. Its appare~t surface diameter was about 110 nm 

(200 km). The eddy appeared to have ~aintained its circulation 

des~ite contact with the Gulf Stream from JuLy to September. The 

Q~lQQQr~k made an XBT temperature section through eddy 76D and 

the GuLf Straam on 5-6 Septe~ber (FilS. 15.13, 15.14). A"lthough 

there is considerable exchange betNeen the Gulf Stream and 

264 
shallow eddy water, the deeper circulation seemed to be closed. 

The sharp ther.mal front on the shoreward side of the eddy 

(Fig. 15.14) indicated considerable velocity shear. In 

mid-December, the eddy was located at 70W30' and had an apparent 

surface diameter of 80 nm (150 km). This eddy persisted into 

1977 until captured by the Gulf Stream during February. 

Eddy 76E (Fig. 15.5) formed about 28 May at 62W from an 

elliptical meander that looped westward from 60W. Its apparent 

surface diameter at this time was about 80 nm (150 km). This 

eddy survived at least into late July, when it became masked by a 

large area of warm surface water. It may have lasted through the 

better part of August, but the fate of eddy 76E is obscure. 

Presumably, it coalesced into either the Gulf Stream or eddy 76D. 

Eddy 76F (Fig. 15.6) formed from a northward extending meander at 

64W on 15 October. Its apparent surface diameter was about 80 nm 

(150 km). It survived until February 1977. 

Eddy 76G (Fig. 15.7) formed about 

had looped westward from 65W with 

90 nm (170 km). After initial 

remained fairly stationary during 

persisted untj l well into 1977. 

27 October from a meander that 

an apparent surface diameter of 

westward movement, the eddy 

December at 67W30'. This eddy 

ZONAL ANALYSIS OF EDDY POSIT I ONS AND MOVEMENTS 

A zonal analysis of all the eddies in 1976 is summarized in 

Table 15.2 to reveal their movements relative to one another. 

The region studied was divided into eight zones of about equal 

lengths along the axis of eddy movements (Fig. 15.15). The zonal 

boundaries were drawn approximately normal to both the mean 

position of the Gulf Stream's north wall and the 100-fm (180-m) 

isobath. The zone in which each eddy occurred at the middle of 

each month is shown in Table 15.2. 

Eddy positions with respect to zone were also determined for 1974 

and 1975 from Bisagni (see footnote 2). The last column of 

Table 15.2 gives the number of occurrences at midmonth for the 

years 1974-76 in each zone. Thus, in zone 4, eddies were present 

at midmonth 15 times out of a possible 36. 

Except for zones 1 and 8, overall eddy activity was fairly 

uniform with respect to zone for the years considered. There are 

relatively fe~ occurrences in zone 8 because many eddies never 

get' that for and those that do are soon incorporated into the 

Gulf Stream. The low leve l 'of activity in zone 1 seems to be 

real, even though partly a data artifact caused by excessive 

cloud interference in the satellite coverage. Occasional cloud 

265 
Paper 15 

free imagery indicates that Gulf Stream eddies are common in the 

Slope Water region east of zone 1. It ap~ears, therefore, that 

eddies formed east of zone 1 (off the centraL Scotian sheLf) tend 

not to move westward very far. No eddies observed during 1976, 

in the area of our analysis, originated east of zone 2. 

A westward boundary to the region of eddy formatiun is apparent 

in the zonal analysis. During 1974-76, no eddies originated west 

of zone 5. 

ENVELOPES OF EDDY CENTER POSITIONS AND BOUNDARIES 

Envelopes drawn around all the observed surface center positions 

and surface boundary positions of eddies during 1976 appear in 

Figure 15.16. The narrow portion of the enveLope of centers 

between 69W and 72W reflects the fact that few eddy observations 

were mad e in this region. 

DISCUSSION 

Satellite imagery has proved itself 

monitoring 

limitations: 

anticyclonic eddies but 

an effective 

does have 

means of 

inherent 

1. Imagery reveals what is happening at the surface, but 

the surface is the last place to become disconnected in 

anticyclonic eddy formation (Gotthardt 1973), whereas the 

area of maximum energy may be over 1JO m below the surface 

(Khedouri and Gemmill 1974). Thus, a feature located near 

the Gulf Stream may appear as a meander in satellite 

imagery, while the main body of water beneath the surface 

circulates as an eddy. 

2. During the summer, surface temperatures ir the Slope 

Water may approach that in the eddies, causing the latter to 

"disappear" in the imagery. This effect probably contributed to eddy 76C's not being detected until mid-August 

(Fig. 15 .. 3). 

3 • The r.e 9 ion 0 f 0 u ran a l y sis iss u b j e c t to l 0 n g per i 0 d s 0 f 

cloudine~s during which eddies may be formed or destroyed. 

Potocsky (1976), in an evaluation of imagery over the entire 

western North Atlantic, found that cLoud free coveraae was 

best during April and October and worst during Decembe;. 

4. Eddy surface expression can be distorted by entrained 

Shelf Water (Potocsky 1976). Chamberlin (see footnote 3) 

266 
sug~ested that distortion may also occur when wind causes 

overrunning of an eddy by surrounding water, or chilling of 

an eddy at the surface. 

This report and that of Bisagni (see footnote 2) demonstrate that 

eddies have a variable, Jut major, influence on physical 

conditions in the Slope Water. During the three years of record, 

the number of eddies oresent at any time has ranged from a low of 

one (November 1974 to mid-January 1975) to as many as six (early 

November 1975; one of which, 751, was not recorded by Bisagni). 

SUMMARY 

Twv well-developed anticyclonic eddies (751 and 76A) occurred 

south and southeast of Georges Bank in the early months of 1976, 

but these were short lived. Only three eddies moved westward 

beyond Georges Bank during the year (76B, 76C, 76D). Although 

two of these, 76B and 76C, were apparently weakly developed, the 

former probably moved at least to the vicinity of the Hudson 

Canyon, and the latter to the latitude of Virginia. Eddy 76D was 

st.rongly formed. It moved to the vicinity of the Hudson Canyon 

by the end of the year. 

ACKNOWLEDGMENTS 

In the National Environmental Satellite Service, NOAA, Franklin 

E. Kniskern provided several prints of NOAA-4 satellite imagery 

and Robert L. Mairs provided 3-hourly ' imagery from the Geostationary Orbiting Environmental Satellite. Rudolf J. Perchal, 

u.s. ~aval Oceanographic Office, provided up-to-the-minute 

satellite information at times when research vessels were making 

special observations in eddies. Philip L. Richardson, University 

of Rhode Island, provided NOAA-4 satellite pictures for the 

February-April period. 

Henry w. Jensen provided special X8T observations south of 

Georges Bank from RV ~lQ£lrQ~~ l~ on 2-3 April. Special acknowledgment is owed for data provided by the crews of cooperating 

foreign fishery research vessels: the German Democratic 

Republic's RV ~rD~l ti£~£~~! for Nansen bottle data on 2~ March, 

the Polish RV ~i~£~QQ for XBT data on 4-7 April and for Nansen 

bottle data on 7-19 April, and the U.S.S.R. RV ~~!QgQr§~ for 

Nansen bottle data on 17-19 A~ril and for XBT data on 5-6 

September. W. Redwood wright and Patrick J. Twohig, NMFS, WOOdS 

Hole, MA, assisted in obtaining oceanographic aata fro~ the 

foreign vessels. 

267 
Paper 15 

Reed S. Armstrong, National Marine Fisheries Service, 

v3luable oceanographic advice. 

gave 

LITERATURE CITED 

bISAGNI, J. J. 

1978. Passage of anticyclonic Gulf Stream eddies through 

deepwater dumpsite 106 during 1974 and 1975. In J. R. 

Goulet, Jr. and E. D. Haynes (editors), Oce~n variability: 

Effects on u.S. marine fishery resources - 1975, p. 293-298. 

u.S. Dep. Commer., NOAA Tech. Rep. NMFS Circ. 416. 

COOK, S. K., J. J. BISAGNI, and K. A. HAUSKNECHT. 

1976. A survey of an anticyclonic (warm core) 

eddy. Gulfstream 2(3):6-7. 

GO TTHARDT, G. A. 

Gulf Strearr. 

1973. Gulf Stream eddies in the western North Atlantic. u.S. 

Naval Oceanogr. Off. Tech. Note 6150-16-73, 42 p. 

KHEDO URI, E., and W. GEMMILL. 

1~74. Phy£ical properties and energy distribution of Gulf 

Stream eddies. u.S. Nav3l Oceanogr. Off. Tech. Note 6150-

22-74, 25 p. 

POTO CSKY, G. 

1976. Ap plication of VHRR-IR satellite imagery 

tatively estimate subsurface thermal structure. 

Oceanogr. Off. Tech. Note 3700-48-76, 18 p. 

to quaLiu.S. Nava l 
I;, 

Table 15.2.--Eddy pos itions at midmonth with resp ect to zone during 1976. The last column 

gives the total number of midmonth occurrences in each zone for the years 1974-76. Zones 

are given in Figure 15.15. Surface boundaries, as seen on satellite imagery, are shown for 

some positions. 

1974-76 

JAN FEB MAR APR MAY JUN JUL AUG SEP OCT NOV DEC monthly total 

1. 3 

2. 76E 76E 76F 76F 11 ~ 

0) 

~ 3. 751 76A 76D 76F 17 

4. 751 751 76C 76C 76D 76D 76D 76G 76G 15 

5. 76B 76B 76C 76D 76D 16 

6. 76B 76C 76D 12 

7. 7sE 75E 75E 76C 11 

8. 76C 3 
,,~ 

, 

/00 -

Figure 1.5. I.-Track Iin«.> for • .nticyclonic ('dd~ I.U: (~:J .Juh I~/.;·~/ \lurd1 l' 71,) • ·urr.we tx,undarlt ' • 

... ho\\n ror "'um po"ltion. 

o~ / 

.-

() ./ 

~ .... ./ 

40° 

~..., " ) 

I 

I 

/ 

I , 

I 

'" rJ 

38° 0 / ,0 

( 

I ~ 

>--

I 

r 

40 " 

4 0c 

38° 

Figure 15.2.-Track lines for anticyclonic eddies 751 (l November 1975-17 March 1976) and 76B (l April 1976-?). Surface boundaries, as 

seen on satellite imagery, are shown for some positions. 

270 
75 0 700 65° 

42 0 42° 

I 

/ 

/ 

/ / 

~/ 

/"1. -/ 

~ 100 - / 

400 40° 

Figure 15.3.-Track lines for anticyclonic eddies 76A (22 February-30 March 1976) and 76C (19 April-15 October 1976). Surface boundaries, as seen on satellite imagery, are shown for some positions. 

Figure 15.4.-Track line for anticyclonic eddy 76D (20 May 1976-February 1977). Surface boundaries, as seen on satellite imagery, are 

shown for some positions. 
I. ur 

"., 

) 

• 

100 

Tr I k Itn f r nU \( I nl Ni 

, 

I 

, 

I 

., 

, 

, 

Fi~urc 1.3.6. -IT Hk line fur Bn ll \ 1001 dd\ i I (I 0 I Ix r I 

(or 

'I 

/ 

/ 

,,~' , 

, 

/00 '-

, 

, 

, 

I , 

, 

, 

, 

, 

,'-, - ........ f_'" I -

urf 

,.~' O~\ : I ' " I \ I -. , 

\ 12,4 \',' ,,' 

, -- ' .. --

2 

o 

2< 

Figure 15.7.-Track line for anticyclonic eddy 76G (27 October 1976-13 !\Iay 19i7). urface boundarie . a !!E'en on atellite imagl'f)·. a 

shown for 80mI' positions. 
36° -~ , , '-- FEBRUARY 28 o 1# 

0 ' __ ,0 

/ 

,/ 

40° ..... -- .,; 

1 '-'I 

/ MARCH 27 0 I .. '" 

1 

I 

I APRIL 14 , 

, 

00' - ~ "' -

"-~ 

I 

, " APRIL 18 

I 

/ APRIL 24 

0' /,0 

36° 

F 

40° 

G 

H 

Figure 15.S.-Interactions between Gulf Stream eddies and the Gulf Stream during the late winter and early spring of 1976. 

See text. 
o 

100 

(f) 

0::: 

W 200 

IW 

~ 

I 

I- 300 

a.. 

W 

0 

400 

500 

A 283 

284 

325 324 275 280 282 285 286 

6 

68· 

GEOR~GES A. BA NK . 

\ 

4 0 · . ~ - -' \ \ \ 

" \ 

~\ 

1/ 1-, \ 

68· 

o 

4 0· 

\ 

50 

NAUTICAL 

288 290 

100 

MILES 

Figure I ;;.9. Expendable bathythermograph (XBT) section (degrees C) from RV A lbatross IVin Gulf Stream meander (or eddy) on 2-3 April 

I ~l7fl that had been pushed into proximity with Georges Bank. Section is not given for line B to C on inset map. The three dots on the map 

inset corr('spond to the locations where the thermal front was defin ed by the XBT survey. See text for discussion. 
-(f) 

0:: 

W 

~ 

w 

:E 

x 

~ 

a.. 

w 

o 

a 

o ~ B i ~7 j ,.. • • I I I 

100 

200 

300 

, 

, 

, 

\ 

, 

18.5 

\ 

\ 

• 

• 

• 

\ . 

\ 

\ 

\ 

• 

• 

• 

• 

• 

• I 

• 18.5 

\ 

• 

• 

• 6~· ,. 

, .. .... GEORGES BANK 

, 

, 

, 

400 " . 

500 , ',- >. • 

o 50 

NAUTICAL MIL ES 

b 

B 

I 

o i~7 j J II • • • I e, 

50 

100 

150 

200 

250 

300 

350 

40· 

400 

450 

• 

• 

• 

• 

• 

• 

I 

• 

• 

• I 

36.2 36.

4 

: 

I 

.. 

I 

I 

~ 

\ 

\ 

" 

• 

• ,

36.5 

I 

" 

I 

• \ 

• 

• 

• I 

500 'i ) i ,. ' , ',. \ , • i • I 

o 50 

NAUTICAL MILES 

Figure 15.10.-Temperature (degrees C) and salinity (%0) sections (a and b, respectively) in eddy 76A on 20 March 1976 from RV Ernst Haeckel. Data from Nansen bottle casts. Depths are 

according to wire length, uncorrected for wire angle. 

tv 

--J 

--J 

a b 

A 8 C A 8 C 

I, 

0 

200 

400 

en 

a: 

w 600 

~ 

W 

~ 800 

I 

~ 1000 

CL 

W 

0 1200 

1400 4~ 

35.0 

1600 

a 100 200 300 o 100 200. 300 

NAUTICAL MIL E S 

Figur(' 15 . 12.- Temperature (degrees C) and salinity (%.) sections (a and b, respectively) on 17 -19 April 1976 from RV Belogorsh. See Figure 15.8G for station locations. Data are from Nansen 

bottle casts. Depths are according to wire length, uncorrected for wire angle. 
A 

o 

100 

200 

Cf) 

a:: 

w 

~ 300 

W 

~ 

400 

:c 

~ 

a.. 

w 500 0 

600 

700 

'0 

w~ U>- 36 «~ LL- a::Z 34 

~-

Cf)-l 

« 32 

Cf) 

0 50 100 150 200 

NAUTICAL MILES 

Figure 15.13.-Expendable bathythermograph section (degrees C) and surface salinities ("/_) through eddy 76D and the Gulf Stream on 5-

September 1976 from RV Belogorsk. See Figure 15.14 for detail of upper left corner of section. Location of section is shown on inset map. 

278 
45 3 5 

o 

if) 

0:: 

W 

f- 100 

W 

~ 

I 

fCL 

W 

0 

200 

o 10 20 30 4 0 50 

NAUTICAL MILES 

Figure 15.14.-Detail of upper left corner of Figure 15.13. 

279 
o 

,,0 

. . .. . 

ME A N POSITION 

Figure 1.'i.15.-Zonr, u,ed in Tablr 1.;.2. 

ENVELOPE OF EDDY 

CEN TER POSITIONS 

ENVELOPE OF EDDY 

SURFACE BOUNDARIES 

o 

cd' 

... ... 

. ... . .. . .. . 

• '0 ' 

Figure 15. 16.-En \'e lopes of surface bounda ri es and center positions of eddi es during 1976. 

280 

o 

c2 
Paper 16 

RIVER RUNOFF ALONG THE MIDDLE ATLANTIC COAST IN 1976 1 

Elizabeth D. Haynes 2 

'rhe river runoff (rate of volume flow) presented here is 

c alculated from the continuously recorded water level at gaging 

stations located at Trenton, NJ, on the Delaware River, 

Poughkeepsie, NY, on the Hudson River, and along the shores of 

Chesapeake Bay at the sections shown in Appendix 16.1. Trenton 

and Poughkeepsie are upstream of any tidal influence, but the 

tidal flow and consequent mixing need to be accounted for in 

order to estimate Chesapeake Bay runoff. 

The unusuaL warming in January and February caused higher than 

average runoff in February in alL three estuaries. Spring runoff 

normaLLy peaks at the mouth of the Chesapeake Bay in March and 

continues high in ApriL as a resuLt of snow meLt i n the southerLy 

James and Potomac river basins, in contrast to DeLaware Bay, in 

which the average runoff is greatest in ApriL, with March a cLose 

second. 

By March there was no snow nor river ice Left in the drainage 

areas, so runoff was unusuaLLy Low. ApriL was hot and dry, with 

less than 50% of normaL rainfaLL and temperatures reaching the 

mid-90's; runoff was Low (Appendix 16.1, Fig. 16.1). Flow 

continued beLow average through May, and then was essentiaLLy 

average in magnitude (within 10,000 cu ft/s 3 of the long-term 

mean at the mouth of Chesapeake Bay) untiL October. 

Due to a succession of frontal waves, rainfaLL in September 

exceeded 150. of normaL. On one day, 5 inches of rain feLL in 

the Chesapeake drainage basin. This weather pattern continued in 

October and brought three times the rainfalL normaL for the mont~. 

IThe data used in this report were suppLied by the u.S. 

GeoLogical Survey District Offices in Hudson, NY, Trenton, NJ, 

and Towson, MD. 

2Resource Assessment Division, National Marine Fisheries S~rvice, NOAA, Washington, DC 20235. 

31,000 cu ft/s = 28.32 m3 /s. 

281 
.jSo 

0 

"V) 

o 

"V) 

. ... . 

6 

ME A N POSIT/ON OF 

o 

,,0 

o 

V) 

Co 

.. 

. . 

.... . 

Fi~lIn' \',.1:; ZUlll" u",d In '1111,1 I i ~. 

0 0 

~Oo "V) ,,0 

<:::) 

ENVELOPE OF EDDY 

CENTER POSIT/ONS 

ENVELOPE OF EDDY 

SURFACE BOUNDARIES 

0 .jSo 0 

1\.0 ~ 

'," . . 

. . . . . . . . . . ~ 

o 

c2 

0 

V) 

Co "1S0 

• ·0 ' 

. . . . . . . . . 

0 

° Co 

Figur e 15.16.-Envelopes of surface boundaries and center positions of eddies during 1976. 

280 

o 

CoO 

0 

° Co 

"10 0 
Paper 16 

RIVER RUNOFF ALONG THE MIDDLE ATLANTIC COAST I J 19 6 

Elizabeth D. Haynes · 

he river runoff Crate of volume flow) presented here i s 

calculated from the continuousLy recorded water Level at g ag in g 

stations located at Trenton, NJ, on the DeLaware Ri r, 

Poughkeepsie, NY, on the Hudson River, and along the s hor s 0 

Chesapeake Bay at the sections shown in Appendix 16.1. Tr n 0 

and Poughkeepsie are upstream of any tidal infLuence, bu t 

tidaL fLow and consequent mixing need to be accounted f o r 

order to estimate Chesapeake Bay runoff. 

The unusual warming in January and February caused hi g he r t han 

average runoff in Febru~ry in all three estuaries. Sprin n r uno f f 

normalLy peaks at the mouth of the Chesapeake Bay in Ma rc h and 

continues high in April as a result of snow me Lt in thp out e rl y 

James and Potomac river basins, in contra st to DeLaware Ba y, ; n 

which the average runoff is greatest in Apr il, with a rch a e l os 

second. 

By March there was no snow nor river ice Left ln th e d r ainag 

areas, so runoff was unusuaLLy low. ApriL was ho t a nd d r y , i th 

less than 501. of normal rainfalL and temperatur es r eac i ng h 

mid-9u's; runoff was Low (Arpendix 1 6 .1, Fi 16 . 1 ). FLow 

continued beLow average through May, and t he n .a s essent; lly 

average in magnitude (within 10,JSO cu ft/ s of the Lon - ter 

mean at the mouth of Chesapeake Bay) until Octob e r. 

Due to a succession of frontal waves, rai n fall i n S per 

exceeded 150. of normal. On one day, S inche s o f r ain fell ;n 

the Chesapeake drainage basin. This we a ther a tt e rn con inued 1 

October and brought three times the rainf a ll no r al for t 

montt"-o 

IThe data 

Geological 

and Towson, 

used in this report ~pre 

Survey District Offices in 

li). 

s u pp li ed 

uds , , 

·Resource Assessment Divisi o n, a ti ona l a r in 

Service, OAA, ashin ton, DC 2 235 . 

1,00 cu ft/s = 2 . 32 Is. 

y he U. S . r non , J, 

fis r . e 
Paper 16 

The highest runoff measured at the mouth of Chesapeake Bay 

(350,000 cu ft/sec) for any month since data were first recorded 

in 1950 occurred in June 1972 as a result of Hurricane Agnes, and 

because of it the annual mean for that year also was the highest 

on record (about 130,000 cu ft/sec, Appendix 16.1). The second 

highest annual mean (115,OOC cu ft/sec), although not monthly 

peak, was in 1975, associated with Hurricane Eloise in September; 

the rest of that year was essentially normal. r ean flolol in 

October 1976 (17~,900 cu ft/sec) exceeded th a t of September 1975 

due entirely to extratropical frontal activity. Despite the cry 

months of spring, the annual ~ean flow in 1976 (b4,4( 0 cu ft/sec) 

was the sixth highest of the 25 years of record. Runoff 

decreased in November and was ave ra ge in Decembe r. 

Runoff in the Delaware Bay and Hudson Ri ver (Fig. 16.1) 

paralleled tnat in the Che~apeake due to the same climctic 

conditions during the year. The December flo~ drop ed in the 

Delaware and Hudson Rivers as the onset of the cold winter of 

1976-77 Locked up precipitation in sn~w and ice. Long-term ~ea~ 

monthly runoff figures were not obtained for the hudson River, 

and the 1976 data are provisional. The annua l average of the 

data set is 20,100 cu ft/sec over the period of record. 

Runoff affects estuarine and offshore fishes and shellfishes by 

varying the saLinity, turbidity, disso lved oxygen, ana 

stratification of their environ~ent. Early warming in the spring 

of 1976 was associated with hi~h runoff very early in the year. 

This accentuated the earLy onset of stratification in the near 

shore waters and suppressed oxygenation two months earlier than 

usuaL. The normal summer bi~logical depletion of dissolved 

oxygen Led to anoxic conditions and the sue sequent fish kill in 

J u L y (A r m s t r 01') g, Pap e r 1 7) • 

000 
Table 16.1.--Mean monthly runoff in cu ft/s (0.02832 

cu m/s). A - Hudson River at Poughkeepsie, NY, 1976 

(provisional data); B - Delaware River at Trenton, 

NJ, 1976; C - Delaware River at Trenton, NJ, monthly 

means for 1941-70. 

A B C 

JAN 29200 19770 11850 

FEB 54800 26830 12410 

MAR 42300 16450 19780 

APR 46300 13420 21500 

MAY 41200 12670 14390 

JUN 18800 7490 8544 

JUL 18200 8610 6440 

AUG 20100 8007 6218 

SEP 12200 4800 4995 

OCT 33900 18020 5637 

NOV 23600 10800 9857 

DEC 19300 7476 11970 

2 
60 

50 

40 

. 30 0 A 

CD 

en 

" 20 B '\ 

..... 

- I 

:::l / 

0 c--

0 10 

0 

0 "-

""" 

MONTH 

Figure 16"1.-~lean monthly runoff into tIlt' .'!addl,· \lllOnlll JI'j(hl \ • Hut! on H.Hr t P u hk p". ' . lUi, (pro\l IOnol t I; 

B· Delaware River at Trenlon, :-'",J, In'; c - I) 11I"lIr(' HI"'r at Irent n, for I II-i 

284 
~ ( 

( 

!) 

0 

) 

c 

APPENDIX 16.1 

UNITED STATES DEPARTMENT OF THE INTERIOR 

GEOLOGICAL SURVEY 

in Cooperation with 

STATES OF MARYLAND, PENNSYLVANIA, AND VIRGINIA 

ESTIMATED STREAMflOW ENTERING CHESAPEAKE BAY 

A monthly summary of cumulative streamflow into the Chesapeake Boy 

designed to aid those concerned with studying and managing the Boy's 

resources. For additional information, contact the District Chief , 

U.S. Geological Survey, 208 Carroll Building 8600 La Salle Road 

Towson, Maryland 21204 Phone 301-828-1535 

J anua r y 1, 1977 

400 . 

100 

50 

10 

150 

" " " " " 

Monthly mean streamflow .. 

into Chesapeake Bay (1976) 

Current year -- Average--- ... 

: .. : .. ,':.: .. . ........... . . . :',,'::::. :': ;::::":':.: ...... . . . . .. ...... .. ,,::- .. : : ....... :'. : .. ,::. :.: . :,' ..... .. .., . ... .......... . .. ,':.:'.: ;::.:::: .. •• • 0.,. 

Unshaded area indicotes ronge . :.:.:::.: .: .. .' "::.: :: : .. .: :.. .. : : . . .. : '. ';: :. :::.: : : : . ~ ... 

~:~:::n o~ i9~~:' ;; ~ yl ::'''''''0 ,d .••..•.•..... • >,./C ... .... ;. .. ..• ..• "(::.! ·.:·::1.· : 1-...w .......... ~........;...w.~_.........A ........ _ .. ~ .. · .. L~:.::: +< . :': 1 : .... ~ :, :~~ :~: I .. 

JAN FEB MAR APR MAY JUNE JULY AUG SEPT OCT NOV DEC 

1- I I I I I I I 11~1 I I 1'1 I , n 

100 ~ 

50 

Annual mean st reamflow into Chesapeake Boy by calendar years 

3 0 -.l.~-.L~~..L.-I J I I L~ __ ~_.L-.L.l I 1 

1950 '55 ' 60 ' 65 70 , 75 1980 

285 
ESTIMATED CUMU LATIV E STREAMFLOW ENTERING CHESAPEAKE lAY 

ABOV E INDICA TED SEC TIONS BY MONTHS , DURING 191' 

220 

200 

180 I 

J 

0 I z 160 

0 

U 

I.U 

VI 

QC 

...., 

~ 140 ~ 

~ I ...., 

~ ...., u.. 

u I 

CD 120 ---I I 

J 

u 

u.. ~ 

0 

~ 100 

z 

< 

VI 

~ 

0 

z 

~ 

60 

F M A M J J A SON 0 

286 

'" 0/ 

0.0 

rc 

0..(> 

. 

t-"- C) 

o~ . '- ~, 

\<.0 

\. "C) t- . <..0 

\ 

<.0 \ 

~, 

~o 0 , 0<" 

~o ,0.0 0 1, 

CUMU LA TI VE INFLOW TO CHESADEAKE B \ 

AT IND ICA TED CROSS SECT IONS 

A Mouth of Susquehanna R. 

B Above mouth of Potomoc R. 

C 8e low mouth of Potomoc R. 

o Above mo ut h of James R. 

E Mouth of Chesapeake Say 
ESTIMATED CUMULATIVE STREAMFLOW ENTERING CHESAPEAKE BAY 

Cubic feet per second at section 

YEAR MONTH A B C D E 

1975 January 53,000 60,600 76,400 85,000 97,600 

February 86,100 97,800 124,600 136,200 155,600 

March 83,000 94,500 132,000 151,300 185,000 

April 50,700 57,800 77,000 84,500 96,700 

May 59,000 67,800 93,500 104,100 121,800 

June 42,500 48,000 62,700 68,300 77,700 

July 19,500 24,000 36,000 43,600 56,100 

August 9 ,460 13,000 19,700 23,600 30,200 

September 86,100 97,800 128,600 138,600 155,100 

October 66,700 76,800 99,600 106,000 118,000 

November 42,500 48,000 63,000 68,400 77 ,400 

December 38,100 43,600 54,400 58,700 66,000 

Mean 53,100 60,800 80,600 89,000 103,100 

1976 January 49,300 56,200 82,80 0 96,000 118,200 

February 102,000 114,800 134,90 0 142,700 155,400 

March 64,600 72,200 87,100 93,700 104,400 

April 45,700 51,800 68,200 74,900 85,900 

May 34,800 40,300 47,600 52,000 59,400 

June 39,200 44,700 53,800 61,600 74,400 

July 25,000 29,900 35,800 38,000 41,900 

August 20 ,900 25,400 30,100 31,300 34,300 

September 12,500 16,400 20,200 21,100 22,900 

October 82,400 93,900 135,000 148,500 173,900 

November 38,600 44,200 58,600 64,200 73 ,400 

December 27,200 32,300 45,900 54,400 68,300 

Mean 45,200 51,800 66,700 73,200 84,400 

287 
Paper 17 

CLIMATIC CONDITIONS RELATED TO THE FISH KILL AND ANOXIA 

OFF NEW JERSEY DURING THE SUMMER OF 1976 1 

Reed S. Armstrong 2 

INTRODUCTION 

A massive fish kill in the bottom waters over the middle 

continentaL sheLf off New Jersey occurred during the summer of 

1976. Beginning in Late June 1976, dead or dying fish and 

sheLlfish were sighted off the northern New Jersey coast and, 

through the summer, the fish kiLL area expanded continuously 

southward. Low oxygen or an~xic conditions accompanied the fish 

kills (BulloCh 1976). By mid-September the region of extensive 

fish mortalities covered an area of about 2,100 square miles 

(5,400 km 2 ). 3 

Observations in August 1976 indicated that the fish kill was 

probably related to the presence of excepti onally low oxygen 

concentrations in the bott~m waters on the shelf. 4 By 

mid-October, oxygen concentrations in the bottom waters had 

returned to near normal conditions. Comparison of the August 

1976 data wit~ historic August observations from the National 

Oceanogra~hic Data Center (~ODC) archives indicates the 

te~perature of the waters below the thermocline and oxygen 

concentrations in the surface layer ~ere not unusual in 1976 

11aken from; Armstrong, R. S. 1'177. "Climatic conditons 

related to tbe occurrence of anoxia in the waters off New Jersey 

durin g the summer of 1976." 10. Oxygen DepLetion and Associated 

tnvironmentaL Disturbances in the Middle Atlantic Bight in 

1976, p. 17-35. 1ech. Ser. R. No.3, Northeast Fisheries Center, 

NIVlFS, NOAA 

2.Atlantic Environmental Group, National Marine Fisheries 

ervice, NOAA, Narragansett, RI DZ8b2. 

SteimLe, F. 1976. A summary of the fish kiLL - anoxia phenomenon off New Jersey and its imnact on resource species, p. 5-11. 

In J. H. Sharp (editor), Workshor Report, Anoxia on the Middle 

Atlantic Shelf during the Summer of 1976, Washington, DC, October 

1976. 

40 ata provided by Northeast 

HighLands, NJ 07732. 

Fisheries 

289 

Center, NMFS, NOAA, 
t

aper  

(Fig. 17 . 1) . Therefore, any ph ysical phe nomena related to the 

anoxic condition in the bottom waters must have occurred earlier. 

To define environmental cond i tions tha t might have led to anoxic 

conditions, various sets o f histo r i cal and climatological data 

were examined. The data used and the i r sources were: 

~onthly ~ean river discharge f or t he Dela~are 

Hudson River, ard cumulat i ve d ischarge into 

Sound, provided by the u.s . G~ol al Survey. 

River and 

Long Island 

~orthly mean sea surface tempera ture, compiled from ship 

reports and published in g~l !~ r~gID (National Weather 

Service, January 1975-August 1976) an d in Ih~ §ylf ~!r~gm 

~QD!hl~ ~~mIDg[~ (U.S. Naval Ocean o g raphic Office, January 

1966-December 1974). 

~onthly mean shore station temperat ures at tide stations 

(Sandy Hook, Atlantic City, and Cape May, NJ), acquired from 

the National Ocean Survey, NOAA. 

historical oceanographic station data , including dissolved 

oxygen ooservations, provided by th e National Oceanographic 

Data Center, Environmental Data Servic e, NOAA. 

In 8ddition, data from oceanogra~hic sta tions occupied in the 

~rea in 197~ were provided by the Sandy Hook Laboratory of NMFS 

3nd by the AtLantic Oceanographic and Mete oro l ogical Laboratories 

0f NOAA 'S Environmental Research Laborato ries. 

CLIMATOLOGICAL CONDIT I ONS 

~n examination of climatological records in d icates that spring 

essentiaLly aegan one to two months ear Ly in 19 76. Comparison 

between the mean and 1976 annual cycles o f warmin g and cooling in 

t~e surface waters off New Jersey (Fig . 17.2) indicates that in 

1976 the waters began warming at Least one mo nth earlier than in 

~ny of the precedin~ 10 yea r s (Februa ry vs. March and April). 

The earLy warmin~ in 1976 is also indicat e d in shore station 

water temperature records, ~here at Sa nd y Hook the increase in 

water temreratures in February over January 1976 represented the 

Ldr est warming for those months for the pe riod of record (32 

y ars). Fe r the lonqer record of shore stat i o n temperatures at 

fttLantic City (1912-19cQ, 1923-1961, 19 7 2-1 9 76 ), the JanuaryFebruary 1976 warmin~ was exceeded only on c e (1927). In 

ditlon, the usual sprin9 increase i n r i ve r d ischarge for the 

D La are nd rludson Rivers (Fig. 17 . 3) bega n abo ut two months 

earLy in 1~76, which wouLd cause an ea rLi e r than normal 

fres ening of surface waters over the she l f . Sp rin g increase in 

:2 U 
discharge into Long Island Sound 

These two conditions, early warming 

salinities from early occurrence 

establish stratification of the water 

months early. 

• II.A,..... .... , 

was also two months early. 

and lowering of surface 

of high discharge, would 

column some one to two 

OXYGEN CYCLE AND STRATIFICATION 

The annual cycle of dissolved oxygen in the subpycnocline waters 

is shown in Figure 17.4, which is a compilation of historic 

observations from the NODC archives f~r a 1-deg square off New 

Jersey (39N-4GN, 73W-74W). Also included in the compilation were 

values collected in July 1957. 5 For this analysis oxygen 

measurements at the greatest sa~pling depth for e~ch station with 

bottom depths >20 m and <60 m were plotted by month, regardless 

of year of ohservation, and a mean annual trend was derived from 

the plotted values. Data were available in all 12 months. They 

were obtained from 77 stations (28 cruises, 12 years). 

During fall and winter, cooling at the surface of the Shelf 

waters causes overturnin~, which mixes the waters from surface to 

bottom and raises bottom oxygen concentrations to equal surface 

concentrations. Surface cooling, overturning, and the resulting 

increase in bottom oxygen concentrations typically continue into 

March (Fig. 17.4), when surface warming b egins. ~lso, surface 

salinities decrease as spring ri v er d ischarge increases, 

establishing stratification. The strengthening of stratification 

and its persistence through spring and summer limits vertical 

replenishment of oxygen into the subpycnocline waters on the 

shelf, where dissolved oxygen is nGrmally depleted by biolo~ical 

activity. The persistence of the cold core over the middle shelf 

through spring and summer, and the strong temperature gradient of 

the Shelf Water/Slope Water front over the continental slope, 

provide evidence of limited lateral mixing and oxygen 

replenishment by advection from offshore. The condition of 

limited vertical and horizontal exchange implies that through 

spring and summer the bottom ~ater on the shelf is a somewhat 

stagnant water mass in which utilization of oxygen is greatp.r 

than replenishment. Subpycnocline oxygen values steadily 

decrease (Fig. 17.4) from the on~et of stratification in March 

until surface cooling and overturning begin breaking up the 

stratification in September. 

5WQods Hole Oceanographic' Institution. 1961. BiologicaL, 

chemical, and radiochemical studies of marine plankton. Reduced 

data report, Appendix C to Ref. No. 61-6. 

291 
APPLICATION OF OXYGEN MODEL FOR 1976 

Assuming that the early warmi~g and early spring riv er discha rge 

in 1976 established stratification tHO months earlier than usual 

(January instead of March), and assuming that oxygen depletion 

progressed at typical rates, a trend for subpycnocline oxygen 

concentrations was formulated (Fig. 17.4). In this formulation 

the normal trend curve for the months of declinina oxygen 

concentration& of Figure 17.4 was shifted to the left two months , 

adjusted downward so that the beoinning point coincided with the 

typical January value, and extrapolated for the additional tw~ 

mo n ths. This shows: 1) maximum oxygen c0ncentration was not 

only achieved earlier, but also at a lower value (6.5 ml/l in 

January 1976 vs. 7.1 ml/l in a normal arch); 2) dissolvea 

o xygen fell to 3.0 ml/l in June, which ;s equiv~lent to the mean 

annua l August minimum; and 3) dissolved oxygen continued to 

d ecrease to 0 ml/l in July. Subseyuent to developing this oxygen 

t rend for 1976, some actual observations of suboycnocline oxygen 

con ce n trations were received from ~L (Atlantic Oceanographic 

and ~eteorological Laboratories) surveys as part of the ES~ 

(Ma rine Ecosystems Analysis) New York bi ght Project. The 

corre spondence with the AOML observations (Fig. 17.4) seems to 

supp ort the contention that anoxic conditions resulted from a 

lengt hened period of near stagnati o n in the bottom waters which, 

in t urn, was caused by the onset of s tratification one to two 

mont hs e?rlier than normal. 

An additional feature during the summer of 1976 was the 

oc cu rrence of a d i stinctly larger than normal plankton population 

th roughout the Shelf Waters of the Mid-Atlantic 8ight during 

sprinq, principally because of an unusual bloom of ~gr§!i~m 

p hytoplankton. 8y summer there was a large mass of dead ~~[~ti~m 

ce lls on the New Jersey shelf, representing a larger than normal 

dec aying biomass. The continued high rate of oxygen depletion of 

ear ly summer and the maintenance of anoxic conditions through 

late summer may be attributed to the Large mass of oecaying 

~~ r§!iYm· 

REGIONAL ASPECTS OF THE 1976 FISH KILL 

Anoxic conditions and the resuLting fish kiLL were apparently 

lim i ted tot he. She l f W ate r s 0 f f New J e r s e y and did not de vel 0 pin 

waters of adjacent shelf regions. Historical oxygen observations 

were examined to explain the limited extent of anoxic conditions. 

An analysis similar to the one presented in Figure 17.4 

determined the annual cycle of near bottom oxygen concentrations 

for a 1-deg square off Long Island (40N-41N, 72W-73W). Histo ric 

observations compiled for this analysis came from 96 stations (32 

cruises, 14 years) with obs~rvations in all months except April. 

292 
Off Long Island, as off e~ Jprsey, max; u otto 0 y n 

concentrations norm.:tlly occ r in a rch, dpcreas sprin nd 

summer , and begin rising in Se ternb r. ',; rr,il a r 0 eye 

ew Jersey Shelf Waters, the annual cycle of dissolv d oxyo n 

Long Island reflects the seasonality)f density stratifle n. 

Uxyqen decredse in this 1-deo squa r off Long Isl nd proe d 

more raridly Ouring spring than off e w Jersey, bu l ss "dly 

du rinn summer (Fi g . 5~ ). Sea su rfa ce tem eratur s nd 

dischar e rates into Lonq I s land Soun" and fro the Hudso Riv r 

in 1976 indicdte that stratification shou ld have been sta lis d 

on to two months earlier than normal off Long Island, as i w 

off Ne~ Jersey. Assumin g th~t stratification beca est a lis 

two months earlier than n~rmal, a trend for 197 was ev Lo 

for the waters off Long Island, beginninQ wit h he ty ical 

for January (6.5 ml/l). Th is curve i s shown ln Figur 

along with the one formulated for e w Jers y otto~ w 

~ i v ens i n, i l a ran 0 malo use v e n t s for t h ~ two are a s (t W 0 - 0 n h - r l y 

sprin g a nd comr a r ab Le ~grEli~m bloom) , bottom OXY9 n off Lo Q 

Island should not have gone mJch beloH 2 ml/l in 197 

The oifferences in the annual cycle of oxyg n conc n ratio 

between tr e tw o areas most likely are the result of b hy ric 

conditi ons . A broad bank (4 U- bJ m depth) exists off Long I l nd. 

A similar bank i s present off ~ew Jersey , but it is out 20 

shall owe r. The anoxic condition in 1976 develope on he sh Llo 

bank off Ne w Jersey , ~hich is tre re2ion wh re the Lowest oxy 

typic a lly occu r s (Fiq. 17.1). The thinner su pycnoclin 

off New Jersey would have a lesser olu e of w ter, nd h nc a 

lesser v o lum e f oxygen , than the wat e rs off Long Islan. In 

AU0ust 1949 , a crU;Sf that transitted both areas fou d t e botto 

f the pycnocLine at a depth of about 25 m ov r the b nks of bo t 

le w J e r s e y an d Lon g Is L C' n d . T h ; c k n e s s 0 f the 0 t to a r l y r 

ff New Jersey was only about 15 ~, w er as 0 0 

Lonq Island. hpplying the ratio of t se vatu s 0 0 y 

concentrations, it could ce ar ued that twice as mue 0 

typic ~lly aval lable belo~ the ~ycnocline off Lon Island 

'Jew Jersey. 

SheLf ~at~rs south of ew Jersey (off t 1 DeL~ rva 

a ls o ey~e ri nce early war in in 1976 ?no ould 

unaer influence of t e early, i h river disc arge. 

fish kills no anoxic c nditions in t 

ttricuted t th,m tric oiff rene s. 

PeninsuLa tht cort;nent L shelf is only a 

Long I~land, allo s 

2n 0 n repl nis 

f e ers 0 

f ~ a nual e cl 

, 

off 
I 

r .... I 

PREVIOUS FISH KILLS 

In the same area as the fish kiLL and anoxia deveLopment of 1976, 

three previous fish kiLls have been reported: September througn 

earLy Octobe r 1968 (Ogren and Chess 1969), October 1971 (Young 

1973), and August 1974. 6 Apparently none of these earlier fish 

kilLs was as extensive or enduring as the 1976 kilL. Low oxygen 

conditions in the bottom waters accompanied aLL of the fish 

kilLs. ClimatologicaL records of sea surface temperature from 

shore station reports and discharge rates for the Hudson River 

for the last ~O years (1947-76) were examined for conditions 

simiLar to those of 1976. During this 30-yr period, high 

discharge (arbitrariLy defined as >15 0% of the monthLy mean) 

occurred five times in January (1949, 1950, 1952, 1973, and 

1974), and three times in February (1951, 1954, and 1976). Shore 

station temperature records for Sandy Hook and AtLantic City 

indicated early warming of the water (monthLy mean for February 

warmer than for January) occurring 12 times at Sandy Hook and 9 

times at Atlantic City. No observations were made in 1970 and 

1971 at AtLantic City, which were two of the years of earLy 

~arming at Sandy Hook. Coincidence of earLy warming and high 

discharg e occurred in 1949, 1952, 1954, 1974, and 1976. 

Therefore, these five years had the poten tiaL to deveLop Low 

oxygen conditions as a resuLt of earLy stratification. For the 

30-yr record, the highest warming ra tes and record highest 

discharge in February alL occurred in 1976. Included in the 

years of potential earLy stratification is 1974, one of the times 

of a reported fish kilL, but not incLuded are the other two 

instances. 

A significant point here is that the fish kills of 1974 and 1976 

occurred during summer, but in 1968 and 1971 they occurred during 

faLL. The im~lication is that vpry low oxygen conditions may 

result from either an early spring or a late falL, either of 

which wouLd Lengthen the period of stratification. OnLy surface 

temperatures wer~ examined to determine the Late arrivaL of faLL 

because river discharge in su~mer and faLL is typicalLy small 

(the highest discharge of the 30-yr record for August is less 

than the monthLy means for December, January, and February, and 

the highest discharge for September is about the same as the 

means for December, January, and February). Sea surface 

temperature records from AtLantic City show that August was 

tYricaLLy the warmest month and Septembe r was warmer than August 

onLy seven times from 1947 to 1976. The instances of higher 

September temperatures were in 1948, 1957, 1959, 1965, 1966, 

1968, and 1971. Of these years the highest rate of warming 

'e. J. Sindermann, Northe ast Fisheries Center, NMFS, Hig~lands, 

NJ 07732. Pers. commun., November 1976. 

294 
Pag 

The roLe that pLankton bLooms ~Lay in th 

conditions is not cLear, but they may be a 

generation of ~noxic 

cess~ry ingredient. 

ALthough the occurrence of very low oxygen concentrations i 

bound to have a catastrophic effect on benthic organisms and 

bottom fishes6 perhaps an equ~LLy spvere impact may develop i~ 

the recruitment of fish stocks because of the cumulative effect 

of frequent re.currence of Low oxygen conditions. Conside rin 

12 instances in the last 3G ye~rs ~hen climatic conditions 

have Led to very low oxygen concentrations, such cond; 

occurred every t~o to three years from 194 8 through 

a 9 a; n f r om 1 9b 5 to 1976 < 1 2 yea r S w; t h six po te n t "i a L 

each period). During these two 12-yr ppriods , ~r 

rebuiLding abundances of bottom species might have bee 

Limited. During the intervening five years (196G-64), w 

were no indications of either early spring or Late falL 

any of the years, maintenance of abundance mi 

considerabLy fietter. 

LITERf\TURE CITED 

BULLOCH, D. K. 

1976 . Ocean kiLL in the New York dight --summer 197v . 

water Nat. 1C(1):4-1~. 

OGREN, L., and J. CHESS. 

1969. A marin~ kiLL on New Jersey 

6(2):4-1c . 

YOUNG, J. S. 

reekS. 

1973. A marine kiLL in 

Pollute BuLL. 4:70. 

e Jersey coastal 

nderloo'ater 

waters. 

Und era 
The role that plankton blooms play in the generation of anoxic 

conditions is not clear, but they may be a npcess~ry ingredi nt. 

Although the occurrence of very low oxygen c ncentrations is 

bound to have a catastrophic effect on benthic organism and 

bottom fishes# perhaps an equ3LLy spver impact may dpvelop ir 

the recruitment of fish stocks becaus of the cumula;v effect 

of frequent recurrence of low oxygen conditions. Consirlerin the 

12 instances in the last ~ ye~rs Nhen clim~tic conditions may 

have led to very low oxygen concentratio~~, uch conditions 

occurred evel'Y tll/O to three years from 1'14 throu( h 1Ci59, and 

again from 19b5 to 1976 (12 year s with six roten ial occ rre ce 

e a c h per i 0 d ) • D uri n g the set W 0 1 - y r rio d s , r s~ , e c t s for 

rebuilding abundances of bottom species might ave bee sev rely 

limited. During the intervening five years (1960-64), wh en ther 

were no indications of either early sprino or late fall ' ills ln 

any of the years, maintenance of a u ddnce t have e n 

consi derably ~etter. 

LITERATURE CITED 

BULLOCH, D. 1<.. 

1976 . Ocean kiLL in the 

water Nat. 1C(1):4-1t::. 

ew Yor digh --summ r 1 76 . 

OGREN, L., and J. CHESS. 

1969. A marin . kill on New Jersey 

6(2):4-12 . 

YOUNG, J. S. 

wrec s. 

1 973. A rna r i n e k ilL i n 

Pollute BuLl. 4:70. 

ew Jersey coastal 

296 

II n e rw ate r 

.... aters . 

Under -

. at. 
-

- 25 

:r: 

fa.. 

W 50 

o 

-

~ 25 -

:r: 

fa.. 50 

w 

0 

75 

AUGUST 1949, ALONG 39°50' N. LAT. 

TEMP. (OC) 

.. 

. . . . .' ~. 

o 

0 

25 50 75 100 o 

DISTANCE 

AUGUST 1976, ALONG 

TEMP. (OC) 

.. " ., . . . ' .. " .. .. ," " .. ' .. ' . '.: .. ... . 

' .. 

. . . . 

25 

. . " . ...... ' . 

. '. . . ... 

50 75 

50 

100 

DISTANCE 

o 

OXY. (mill) 

25 50 75 

( k m ) 

39°30'N. LAT. 

OXY. (mill) 

.... . .' 

.. " . . . 

.. . : : .:" ..... " .. ' 

" . . , . "'. 

.... ', .... ,',', .. . . . . . ... '. 

. . 

100 

25 50 75 100 

( km) 

Figure 17.1.-Temperature and dissolved oxygen structure off central New Jersey (August 1949 data from National Oceanographic 

Data Center archives; August 1976 data from Sandy Hook Laboratory, NMFS). 

297 
+10 

J 

-() 

0 

- (!) 

~ z w - (!) +5 RANGE OF EXTREMES ~ z 1966-/975 0:: <{ <{ ::r: 

() 3: 

w 0 0:: 

~ (!) 

r z <{ - 0:: -5 .J 

w 0 

a. 0 ~ () 

w 

r -(0 

Figure 17.2.- Monthly sea surface temperature change, July 1975-August 1976, and its historic 1966-75 range at 39N-40N, 73W-74W 

(values from gulfstream, National Weather Service, NOAA, January I975-August 1976, and The Gulf Stream Monthly Summary, 

U.S. Naval Oceanographic Office, January 1966-December 1974). 

70 D J I 70 D 

(f) 

LL RECORD FOR u 

J') 60 RECORD FOR MONTH 60 MONTH ~., 

0 1941-1970 1947-1975 ____ ., 

w 50 ". 50 . c:> " . '. ". 

0:: . c:{ 40 . 

. 40 :z: , u 1976 

(f) ..... 30 ~ " 0 .' 30 " / ,.' " ~ " 20 20 ----"" :z: 

tZ 10 10 29 YR. MEAN 

0 1947-/975 ::E .30 YR. MEAN-1941-1970 

0 0 

DELAWARE RIVER (TRENTON) HUDSON RIVER (POUGHKEEPSIE) 

Figure 17.3.-Monthly river discharge rates for 1976 and long·term means and extremes (from IT S. Geological Survey provisional 

records). 

298 
8 N N 

-....J 

"-

7 E 

- 6 ... : .... . Z \ RANGE .. OF W 5 

(!) OBSERVATIONS 

>- (FROM N.O.D.C. HISTORIC DATA FILES) 

X 4 

0 

I OBSERVATIONS BY 

0 3 AOML IN 1976 

W 

~ 2 

0 

(f) 1976 TREND 

(f) 

0 

0 

Figure 17.4.-Subsurface (>20 m) dissolved oxygen as predicted and observed in 1976 and historical range and mean at 

39N-40N, 73W-74W. 

299 
~ 

8 

8 

(a ) 

7 

6 J ~ 

-..... 

C 5 

w ,/ V') 

~ 4 / UJ 

cr / u 

uJ 

Cl ~ 

z 3 / ? w 

L':' LO',G ISLA'ID >-

>< 

0 ..0 2 

o 

o 

~lUl'I~ER :':O~lTHS AFTER OXYGEN I,IAX !:-lU' 

Fij{uro' li,Ii, Tn'nds or h"lIom OX)I("I\ lind It ... monlhl,\ d.'crt'us" 01T ~,-" 

DIIIII I't-nll" IIr,'hi\('d datu IlIHI ('~I,·n.It"1 for U pr"lonl{.-d ''''rlot! 

8 

I (b ) 7 

6 

-I 

.... 

,.... 

!'. 5 

l •• 

1..') 

>-

X 

C) "LO';S I SLAN~ C) 

1.J 

:~ 3- 'lEW JERSEY ~ <.. " Vl 

T V') " .-

Q 2 I ~]S[R'!A'" rOl,s BY " 

o I 

7 JA' 

phil" 

ror 1 
Paper 18 

VARIATIONS IN THE POSITION OF THE SHELF wATER FRONT OFF THE 

ATLANTIC COAST BETWEEN GEORGES BANK AND CAPE ROMAIN IN 1976 

John T. Gunn ! 

INTRUDUCTION 

Dup to the tendency of forage organisms, and thus pelagic fish 

tocks, to be associated with the convergence zone of ocean 

fronts, knowle.dge of temporal and spatial variations of the Shelf 

water front position can be imDortant to fishery scientists. 

Because the Shelf ~ater front may extend to the bottom over the 

continental shelf, there is also the possibility of an effect on 

oenthic and demersal species. It is anticipated that a better 

understanding of the interaction of different species with ocean 

fronts also may lead to more efficient fishing efforts. 

This report is a product of a monitoring effort using infrared 

satellite imagery which records ther mal features of the sea 

surf?ce. Previous reports (Ingh?m 1976; Gunn 1978) have discussed front variations from June 1973, when data first became 

avaiLable, through 1975. This report wiLL discuss the data for 

1976 and its comparisons with previous years. 

DATA 

The basis of this study is the Experimental Gulf Stream Analysis 

Charts 2 (Fi~. 18.1), drawn fron the best infrared NOAA satellite 

image of the ~eek or, if large ~aps occur on daily charts due to 

clouds or observational limits, a composite of several partial 

images. These charts show the position of the surface thermal 

boundaries between the followinq oceanic features: Shelf Water, 

Slope ~ater, Gulf Stream, and warm and cold core Gulf Stream 

eddies. 

l AtLantic Environmental Group, National 

Service, NOAA, Narra9ansett, RI 02882. 

2Proauced by EnvironmentaL Sciences Group, 

mental SateLLite Service, NOAA, Washington, DC 

Marine 

National 

20233. 

Fisheries 

Environ-
Paper 18 

DATA ANALYSIS 

To portray the vari a tion o f the She lf Water frontal position, 

distances were measured to the f ro nt along 12 standard bearing 

lines from selected coast a l po ints ( Fig. 18.2). These bearing 

lines intersect the 2C8-m i so ba th at regular intervals <about 

150 km) and are approximately perp e ndicular to it. The distances 

measured from each satel l ite c h art are corrected for scale 

variation (+ or - 5%) from chart tJ chart and converted to 

kilometers. These distances a r e t hen red u ced by the distance 

a Long each bearing line to the 200-m isob at h. The resulting 

values represent the distance from t he shelf edge, as defined by 

the 200-m isobath, to the front; posi tive values are seaward 

fro m t his i s ob a t h • 

Al so, a measurement of the i ntrusion of Slope Water over Georges 

Ban k was produced by mea s uri ng th e a rea covered by the Slope 

Water on an overlay of the 200-m i s oba th . For this calculation, 

Georg es Bank was defined a s th e are a of the bottom at a depth 

<zeD m and ea s t of 69W in th e Geo r ges Bank region. The 

intru sions are expressed as a percentage of the Georges Bank area 

cover ed by Slope Water. Chart to chart scale variations are 

partly com~ensated for by using various s caled overlays. 

WEEKLY FRONTAL POSI TION S 

Inspect ion of the weekly fro nt al po s itions along a bearing line 

can suggest occurrences o f excursi on s o r intrusions and general 

spatia l and temporal trend s . Compa r is on between adjacent bearing 

lines allows the identification of ev e nts which affect more than 

one bearing line. Inspection of th e in div idual weekly charts 

suggests possible causes such as Gul f Stream meandering or warm 

core eddies. The discussion of th e d ifferent bearing lines is 

broken up into three regions: New Eng l a nd, Middle Atlantic, and 

Southern, in order to simpl ify di scussion. There is some 

evidence in the dat2' howe ve r, J f cohesiveness among the 

differen t groups. 

~g~ £Dglgrr~ - The three nort he rnmost bearing Lines (Fig. 18.3), 

originati ng from Casco Bay , ME, e xtend into the region where 

Large amplitude GuLf Stream me a ndering and warm and cold core 

eddy produ ction cause large fluctuations in the Shelf Water front 

posi tion. Since the lengt h s cales of these phenomena are 

gene raLly equal to or l ess than twice the separation of the 

oea rin g lines, this can lea d to a biasing of the data and 

conseque nt misinterp r eta ti o n. Consider, for example, the 

February-~arch period on the Ca sco Bay bearing lines. The graph 

of Casco Bay 120 ind i ca tes an intrusion which pea~s at the 

beg innin g of ~a ch. Th e g r a ph of Casco Bay 140 indicates an 

302 
xcursion that peaks at the same time, and the third graph, Casco 

ay 160, show~ a gradual offshore to onshore trend. The dlstance 

letween the peak excursion and intrusion was approximately 

50 km. Inspection of the weekly charts shows the formation of a 

arge warm core eddy at the beginning of February. The Casco 

ay 120 bearing line crossed the eddy and thus showed an 

ntrusion of the front. The Casco Bay 140 bearing missed the 

~ddy, but hit an area of Shelf Water entrained by a previous 

~ddy, and thu~ showed an excursion of the Shelf Water front. The 

:asco Bay 160 bearing line measured a more realistic mean trend. 

hus care must be used 'when interpreting short period 

fluctuations. Note that a similar occurrence took place in 

nid-July. L~nger period trends are more reliable on these 

earing lines,. and better correlation exists from one bearin~ 

line to the next. The 2 1/2 month intrusion which showed up on 

the Casco Bay 120 bearing line from July to mid-September was 

au sed by a large meander and warm core eddy formation which was 

also associated with a large increase in the area of Slope Water. 

lthough the Casco Bay 140 line does not show strong evidence of 

his, the other two lines sho~ definite shoreward displacements. 

The Casco Bay 120 bearing line shows the greatest fluctuation of 

the three, with the Casco Bay 140 line showing large fluctuations 

only in the fi rst three months ~f the year, and the Casco Bay 160 

line showing only minor fluctuations during the whole year. 

~iQQi~ A!i20!i£ - This region consists of si x bearing lines from 

Nantucket Island to Albemarle Sound (Figs. 18.3-18.5). On the 

first three bearing lines, Nantucket, Montauk Point, and Sandy 

Hook, a tongue of Slope Nater moving offshore caused large 

fluctuations during January-March. The next event that affected 

a number of bearing lines was a large area of Slope Water formed 

in the begioning of July (also mentioned in the previous 

section). This resulted in a large intrusion observed on all six 

middle Atlantic bearing lines. Cloud cover obscured the event on 

the more southern bearing lines, but it was obvious that a large 

frontal displacement took place. On the Nantucket, Montauk 

Point, and £andy Hook Lines, this displacement appears to have 

lasted until the end of October, interrupted by a large excursion 

of the front in late August. The three most southern bearing 

lines in this region did not seem to recover as well and remained 

closer to their mean positi~ns after this excursion. The 

excursion in late August was sudden, taking place in a week on 

s~me bearing lines. 

~QYlb~rQ - The southern bearing lines suffer from large gaps in 

the data during the summer months due to cloud cover (Fig. 18.5). 

The number and amplitude of ~xcursions and intrusions in this 

region were smaller than on the bearing lines farther north. The 

only well-correlated movement occurred on the Cape Fear and CapE 

Romain lines_ A seaward excursion in late September and October 

303 
Paper 18 

changed to a significant intrusion in Late JovPfT,ber. In pection 

of the weekly charts showed that durinn this reriod, the GuLf 

Stream had me3ndered offshore and a reLativeLy Larq~ area of 

SLope Water forced the SheLf ~ater front to impin~e on th coast. 

MONTHLY MEAN FRO TAL POSITIO JS 

The monthLy mean frontaL positions are shown in Figure 18.6 for 

the three compLete years of data coLLection. Care souL te 

exercised in interpretation since the nUMber of wpe 5 avpr~Qeo 

varies (due to lack of d3ta because of cLou 5, etc.) and 

occasionaLLy only one weekLy value was avai La Le f{lr t e month 

(about 51. of the ti~e). 

Definite tendency for seasonality exists for the bear;nQ Linps 

from Casco Bay 120 to Sandy Hoo . In aLL three years, ~ese 

bearing Lines tend to be more offshore from January to ay than 

they are for the June to Dece~ber ~eriod. There are exce~tions 

to this, such as Casco Bay 12J in 1975, aLso Sandy ook oes not 

hold to this trend as weLL as the other earing lines. However, 

the overaLL tendency was strong. The am Litude of his seasonal 

variation for most of the bearino lines was 30-4G km, although 

variations of 10C-150 km exist . 

Seasonal variation was not as consistent on t~e other bearing 

Lines and on so~e, there was littLe indication of it. The Ca e 

May and Cape Henry bearing Lines show littLe seasonaL variation, 

but seem to be affected by shorter period fLuctuations and 

aperiodic occurrences. The ALhemarLe Souno tezring Line s wed a 

seasonaL cycle in 1974 and 1975, being onshore the first art of 

the year and offshore the latter, but it did not show this cycle 

in 1976. 

The three southern bearina Lines suffer from gaps in 

making it difficult to determine if seasonal var;3tions 

exist on these bearing lines. The three bearing 

correlate welL amonQ themseLves, however, suggpsting 

are affected Qy similar events. 

YEARLY MEAN FRONTAL POSITION 

the data, 

do indeed 

Lines do 

that they 

The yearLy mean shelf front position for 1976 agreed weLL with 

the position for the previous two years (TabLe 18.1; Fig 18.7a) . 

Except for Casco Bay 120 and Sandy Hook, the 1976 positions were 

cLose to those for 1974 ~nd 1975. The Casco Bay 120 mea~ 

position was considerably more seaward (about 40 km) and the 

position for Sandy Hook was sLightly more shoreward {about 

30~ 
5 km). This was also evident in the monthly ean ro l 

ositions (Fig. 16.6) discussed above. It as lso int r tinQ 

n note that the seawaro displacements of the yearly mean frontal 

usition tro~ the Qeneral north-south trend, at ontau Point a d 

a'.:'e lienry, are pvident in all tr.ree years. 

he variability of the front, as reflected by the standard eviaion (Table 1R.1; Fiq. 18.7c), increases in 1976 along the bearnn lines from Nantucket to Care ~enry. Inspection of the we ly 

rontal ~osition graphs seems to confirm this, with greater 

m~litude excursions and intrusions more prevalent in 1976. 

INTRUSION OF SLOPE ~ATER OVER GEORGES BA 

he measurement of the area of Georges Bank covered by Slope 

~ater confirms the seasonality of the sheLf front in this region 

(Fig. 18.8). There are no intrusions of the SheLf ater fron 

over Georges Bank in 1976 before the end of ~ay and no large 

intrusions until July. This also agrees with previous years' 

data. Large intrusions occurred in the latter part of July and 

early ~art of August and September, with maximum coverages of 

21(" 11%, and 16% respectively. Generally, Georges Bank as 

partly covered by Slope Water from July until November. 

This typ~ of seasonal coveraQe aLso occurred in the previous two 

years. 

LITERATURE CITED 

GUNN, J. T. 

1970. Varidtions in the position of the Shelf water fron off 

the Atlantic coast between Cape Romain an Georges Ban in 

1975. Je J. R. Goulet, Jr. and E. D. Haynes (edi ors), 

Ocean ~ariability: Effects on U.S. rrarine fishery 

r~sources - 1975, p. 213-228. U.S. Dep. Co~mer., 0 A T C 

Rf>p. N~FS Circa 416. 

11 GHAf"I, M. C. 

1976. Variations in the sheLf water front of he tl ntic 

coa~t b~tween Cape Hatteras and Geor es Ban. IQ J. 

Goulet, Jr. (compiLer), The environm_nt of the nit St t S 

living marlne resources - 1 74, o . 17-1-- -21. u.s. 0 

Commer., atl. Oceanic Atn,os. d in., a l. are Fi 

erv., 'AR~4P (ar. eSJur. ~onit. ss s. Predict. Pro r ) 

Contrib.1J4. 
Table 18.1.--Sample size, mean separation, and standard deviation of Shelf 

Water front position along standard bearing lines, 1974-76. 

Standard 

Sample size2 Mean separation3 deviation 

Bearing line1 1974 1975 1976 1974 1975 1976 1974 1975 1976 

Casco Bay 1200 30 38 30 45.4 72.2 119.6 70.9 59.0 76.1 

Casco Bay 1400 31 38 33 35.4 0.4 39.7 64.0 22.6 46.6 

Casco Bay 1600 36 41 37 6.1 -2.9 1.1 39·3 26.1 27.3 

Nantucket 1800 37 35 40 0.6 -5.6 -1.1 38.5 37.8 55.6 

Montauk Pt 1500 34 35 41 19.8 8.8 14.5 36.7 38.3 64.8 

Sandy Hook 1300 36 35 43 1.2 -4.4 -17.0 46.8 45.0 57.8 

Cape May 1300 38 34 44 4.1 -7.3 -2.5 31.8 34.8 46.4 

Cape Henry 950 40 32 41 17.4 7.3 6.6 36.4 39.5 47.1 

Albemarle Sd 900 40 31 41 -11.5 -16.7 -17.0 24.6 32.5 32.2 

Cape Lookout 1350 24 31 37 -18.2 -24.5 -17.1 20.1 28.9 19.3 

Cape Fear 1400 19 28 36 -20.2 -35.8 -29.6 40.5 38.4 29.2 

Cape Romain 1400 21 22 32 -9.9 -40.2 -17.5 43.4 3303 35.7 

1 See Figure 18.2. 

2Number of weekly positions of front. 

3Distance (km) of front from 200 m isobath; positive is seaward. 

306 
80 75 

T T 

EXPERIMENTAL GULF STREAM ANALYSIS 

NOAA-2 SATELLITE THERMAL INFRARED VHRR 

Observed: ;1.1-30 APRIL \Q1/.fPLEASE FORWARD COMMENTS TO : 

NOAA-NESS Suite 300 

3737 Branch Ave., S. E. 

Washington, D.C. 20031 

Attn : Environmental Sciences Group 

N-bq 

U.s. 

CAPE 

70 

T 

Slv-l 

S. ~ 

~-r--~~--~--------------+---------35 

+-.,.--- Cold water 

intrusion 

LEGEND 

G.S. Gulf Stream 

W.E. warm eddy 

SIW Slope Water 

ShW Shelf Water 

sharp thermal gradient 

- - - -- less distinct thermal front 

, 

BERMU DA 

d 

30 

25N 

Figure is. I.-Example of weekly Experimental Gulf Stream Ana lysis chart produced by Environmenta l Sciences Group, NESS, 

NOAA, Washington, DC. 

307 
80° 

A. 

V 

, , 

Figure 18.2.-Twelve standard bearing lines used in the portrayal of the time variations of the Shelf Water front positions relative to the 200-m 

isobath (dotted line). 

308 
') 

JJ 

300 " - '- /976 . CASCO BAY 140 0 ---/975 200 . . . ",' '. . ...... /974 

..... : .. . f. 100 .:....-;;\ . . _/ /' " 

"'~. ;'/\ .' . /, ....... /. 

a /' . '" --.... / 

200 

:. 100 .': CASCO BAY 1600 

::::--- ... ... . / 0\ 

A ~~/~~~~~~~~~~,- A • ~~ /.--/". ·r:~·//' -~-~-~~~~~~~~~~~~~~~ 

-100 

200 

100 

NANTUCKET IS. 180 0 

a ~~~~~-P~~~~~--~~~~~--~~~~~~ 

-100 

J o 

MONTH 

<igure 18.3 .- Annual march of helf Water front positions relati\e to the 200-m isobath (positive i, sea~ardl. 1974-76, along ,tandllrd he rinK 

lines for New England and the Middle Atlantic regions. 

309 
200 

en 100 

0:: 

w a 

~ -100 

W 

~ 200 

0 100 -1 

- a ~ -100 

J 

MONTAUK PT. 

SANDY HOOK 

CAPE MAY 130 0 

.' 

/ ' I 

.... ·><.i.·. I 

.-.. 

. ",/ ./ 

.-' ./ 

CAPE HEN RY 95 0 

MONTH 

_ .- 1976 

- - - 1975 

········1974 

130 0 

., 

' . . . 

\ 

Figure lSA.-Annual march of Shelf Water front positions relative to the 200-m isobath (positive is seaward). 1974-76. along standard 

bearing lines off the Middle Atlantic region. 

310 
~ 

6 

300-r----------------------------------------

200 

100 

o 

200 

100 

0 

200 

100 

0 

-100 

200 

100 

0 

-100 

ALBEMARLE so. 

CAPE LOOKOUT - .- /976 --- /975 ....... /974 

/- ...... "'-. '=--;"... /' .......... ~ ........ ~'<::. -'-"\, "" .~- ...... . ~. /'":.--/ 

CAPE FEAR 140 0 

..... . / 

'."" . . t""" - - ....... " ...... - . . "''v/'' /\ ..... ,'- . I " . '- - i.' - . - . ...... ' . . ,I 

CAPE 

J 

ROMAIN 140 0 

" ... \.-.-...... ---------7~ ... ~----~----~--~ 

o 

MONTH 

l'igure IS.5.-Annua l march of Shelf Water front positions relative to the 200-m isobath (positive i.eawardl. 19i~-i6. along ,tandard bearln!>: 

lines off the Middle Atlantic and southern regions. 

311 
CB 120 

CB 140 

CB 160 

NT 180 

MP 150 

SH 130 

CM 130 

CH 95 

AS 90 

CL 135 

CF 140 

CR 140 

1974 1975 1976 

1 ",-, ._. ._ ."- ..-' 1 // , ......... --. , . / 

_.-. , '-.-"""' _./ ./ 

'-.-' '-. _.- .-., ' . , 

.-./'. . I '1 -- . .- . -'-'-'-'-'-'-'-'1-- '--'-'-'-'-'-'-'-""1' ....... ._./ '-'-'- .-._.-'-'-'--....... .- ~ / '-..-.--' .- -'-'-'- '~.- -'- I - -.-'- ........ _ .- .""", ._ 1 ._ ._ ., ,,' ._._ ./ 

........ -'-,-.,'--T" .-.-'-._.-.-.' I ./ - - --. 

-"----, ----/----1 /--- --.-'--'--'--i-' --._/ / _.-'-- '-._ .- .- -'-.- _.- '- ....... ./ _.-'-._.-. / _.-.-.-.-./ /' -'-. / ' .- .-

1 _ ' , I -"", .- .- __ '_ 0_._.- __ ._. ____ '----"_'_'- '- '- ' ........ ",,'---.. ___ 0_._'_ , "" ---../ - _. 

__ '_ _. '_ I. _. . ....... . -.-.-.-.- --' 1'--. ..---.-. ~ -'

, -..--' '--- /' -- ". '_ . _ __ ~ _ ' _ '_ '_ '_ '_'_._._ - - _ .'" ........ ..--._ ._ ._ - - - - / 0- ......... ~ .......... 

-' ........ '""'- - ' ' ''-0,. .,-

'-.-_._.1._._.-._./ -', ___ .. _._.1._._._._._ --.- -..- - _. I - ' 1 . _ .--. ...-..- ...... - _./ .- .-.-.- ........... . ---.---.---_.- .-

......... .......... -. 

.'-..- .- . 

........ I _._._' I __ ._._. -- '- '-' '-.-.- ' ._-

JFMAMJJASONDJFMAMJJASONDJFMAMJJASOND I 200 KM M 0 NTH 

Figure 18.6.-:\lonthly mean helf 'Vater front positions. relatiH' to :WO-m isobath (po<tthe i, ea" ard). 1 'Ii l-i6. along t ndard b arin 

312 
z 

~( l&J 

~U 

!z 

L..<t 

~.-

'JD CI) 

~ 

W 

~ 

z 

o 

I-- « 

> 

IJJ 

10 

-

0 

100 

50 

0 

-50 

100 

50 

o 0 

2: 

~ en 

A /976 

- -- /975 

\ ••••••• /974 

• • • 

•• • •• • • • • 

•• 

--

CB CB CB NT MP SH CM CM AS CL CF CR 

120 140 160 180 150 130 130 95 90 135 140 140 

B 

~ ..... ........ ,-:-. .~ ~ .. , ... 

Figure 18.7 .-Annual mean Shelf Water front positions relative to 200-m isobath (positive is seaward) and standard deviation of position 

at each standard bearing line, 1974-76. 

313 
o 

W 

0:: 

W 

> 

o 

u 

~ o 

50------------------------------------------------~ 

40 

30 

20 

10 

o 

J 

- ,- · 1976 

---- 1975 

....... 1974 

o 

MONTH 

Figure lS.S.-Percent of Georges Bank covered by Slope Water, 1974-76. 

314 
Paper 19 

TEMPERATURE STRUCTURE ON THE CONTINENTAL SHELF 

AND SLOPE SOUTH OF NEW ENGLAND DURING 1976 

R. Wylie Crist and J. Lockwood Chamberlin l 

INTRODUCTION 

This report continues for a third year a series of analyses 

beginning with 1974 (Chamberlin 1976, 1978) that are intended to 

reveal the principal temperature variations on the continental 

shelf and upper continental slope south of New England, with 

emphasis on bottom temperatures. Includea are the vertical 

temperature sections on which the analysis is based, as well as a 

contoured diagra~ of bottom temperatures derived from the 

sections. Similar bottom temperature diagrams for 1974 and 1975, 

and a lon~-term monthly mean bottom temperature diagram for the 

years 1940-66, are available for comparison in the report for 

1975 (ChamberLin 1978). 

PREPARATION OF VERTICAL SECTIONS AND BOTTOM TEMPERATURE DIAGRAM 

As in previous years, this analysis has depended on the 

cooperation of scientists who made data available from cruises 

that traversed the shelf south of New England in a generally 

north-south direction (Fig. 19.1). Sixteen sections have been 

used (Appendix 19.1), obtained from cruises of eight different 

research vessels. These temperature sections are not from along 

a single line, but from an area up to 90 nm (170 km) wide at the 

southern end centering on about 71WOO' (Fig. 19.1). Am~iguities 

introduced to the analyses by the lack of spatial coincidence 

amon~ the sections have been previously discussed (Chamberlin 

1976, 197d). 

The vertical tempp.rature sections constructed for each transect 

have uniform distance and depth scales (Appendix 19.1). All 

sections were constructed from expendable bathythermograph (XBT) 

lAtlantic Environmental Group, National Marine Fisheries 

Service, NOAA, Narra0ansett, RI 02882. 

315 
data plotted directly from the traces, except section 7 which is 

based on mechanical bathythermograph data. 

The bottom temperature diagram (Fig. 19.2), prepared by the sam e 

method as in previous years, is an inter~retation of where 

isothermal surfaces intersected the bottom throughout the year 

(Chamberlin 1978). 

The occurrence of warm core Gulf Stream eddies, numbered in 

accordance wjth Mizenko and Chamberlin (Paper 15), are indicated 

as duration lines at the bottom of Figure 19.2. The durations 

we re determined from the Experimental Ocean Frontal Analysis 

(EOFA) 2 and from infrared imagery from NOAA environmental 

satellites. The duration lines are based on the same criteria 

u sed for the 1975 analysis (Chamberlin 1978), that is, the start 

of each line is on the approximate day when the western surface 

boundary of the eddy crossed 70w15' and the line ends the day the 

edd y completely passed south of 39N30'. Of the three eddies that 

appar ently passed south of Ne~ England during 1976, only the last 

(ed dy 76D) sbowed a clear surface temperature contrast in the 

sa t e llite imagery, and thus could be tracked with assurance. The 

dura tion lines of the first two (eddies 768 and 76C) are dashed 

in Figure 19.2 because their times of ~assage are rather 

uncertain. Less stron~ly developed than eddy 76D, they showed no 

surf ace temperature contrast in the satellite imagery during 

thei r passages and were detectable only by inference on a few 

occas ions from tongues of Shelf Water projecting into the Slope 

Water in the pattern generally associated with entrainment by an 

eddy . 

HIGHLIGHTS OF TEMPERATURE SECTIONS 

The fo llowing sections are illustrated in Appendix 19.1. 

Secti on 1. NuAA RV ~~l~l Cruise 76-01,4 February. 

Te mp eratures in this short section fro~ the inner shelf were 3C 

cold er offshore to 7C colder inshore than in mid-December, seven 

week s earlier (Chamberlin 1978). The water was mixed to a depth 

of about 20 m. The 1-2C temJerature inversion in the underlying 

wate r indicated the presence of warm Slope Water near bottom on 

the outer shelf. 

Se ction 2. 

Thermal 

NOAA RV ~~l~l Cruise 76-02, 9-10 February. 

structure in this detailed section was unusually 

2Issued weekly by the u.S. Navy Oceanographic Office, Applications Re s earch Division, Suitland, MD 20374. 

316 
complex. In the central part of the section, at depths below 

about 50 m, the vertically nixed Shelf Water was underlain by 

warm Slope Water containing on isolated 12-13C core that 

contacted bottom at depths around 90 m. Additional disruptions 

of the warm SLope Water were revealed by two much larger cells of 

13C water at increasina middepths in the offshore part of the 

section. There was also a marked seaward excursion of the Slope 

Water front at the surface (10C at about 39N3S'). Satellite 

imagery 3 r€vealed this excursion to have been more pronounced to 

the east of the section line. In addition, strong upwelling of 

deep Slope Water, causing marked reduction of bottom temperatures 

below 100-m depth, was evident in the section, as well as in 

Figure 19.2. The isolated body of relatively cold water «11C) 

on the bottom at depths around 130 m indicated that the upwelling 

was subsiding at the time the section was made. Boicourt and 

Hacker (1976) suggested that winds may force offshore transport 

of surface waters, accompanied by a return flow of deep Slope 

Water. The isotherm pattern of section 2 was consistent with 

this type of event, not only in the upwelling of deep Slope 

Water, but also in offshore surface displacement of the slope 

front. Analysis of average montnly wind-driven transport off the 

AtLantic coa£t during 1976 showed an anomal~usly strong offshore 

(southward) component for February in the SLope Water area south 

of New EngLand (Ingham, ?a~er 12). Str ong westerLy winds during 

the passage of a severe storm that moved up the Atlantic coast on 

2 February may have been a factor in the offshore surface 

transport. 

Section 3. NOAA RV 81Q~t[Q~~ l~ Cruise 76-01, 23-24 February. 

The mixed Shelf Water was O.5-2C colder than in the previous 

section, made t~o weeks earLier, and was at the minimum observed 

during the year. The underlying intrusion of warm Slope Water on 

the outer shelf was of similar dimensions to that in the previous 

section, but Lacked an isoLated core Jf water warmer than 12C. 

Section 4. NOAA RV 81QQt[Q~~ l~ Cruise 76-02, 25-26 March. 

The verticalLy mixed Shelf Water, although LittLe changed in 

temperature from a month earlier (section 3), extended to greater 

depth (about 60 m) where the slope front was more withdrawn. 

UnLike the sections from the Late winter of 1975 (Chamberlin 

1978), which £howed temperatures of the warm SLope Water on the 

outer shelf to be at their annual minimum in March (maximum 

<12C), the 1976 sections indicated no such minimum. On the 

contrary, 13C water occurred near bottom, and 12C water contacted 

bottom in each of the FebruarY-~8rch 1976 sections that included 

the Slope Water zone. This continuation of warm Slope Water 

temperatures may be associated with the anomalousLy warm air 

3EOFA (Experimental Ocean Frontal Analysis), 4 and 11 February. 

317 
I

aper 1'7 

temperatures along the Atlantic coast in February and subsequent 

moderate air temperatures during the spring (Dickson 1976; 

Taubensee 1976). 

Section 5. Polish RV ~i~££QQ Cruise 76-01, 10-11 April. 

The first rise in SheLf Water temperatures «1C) was evidenced 

in this section shoreward of the 6J-m isobath. At the bottom, 

the slope front was withdrawn offshore to the greatest depth 

observed during the year. As a result, bottom temperatures were 

at their observed annual mininun in depths of BO-15C m. 

Se c tion 6. Duke University PV ~£~1~2rQ Cruise E2876, 11-12 May. 

De v elopment of the seasonal thermocline had defined the 

underlyin g cold core which ha d a temperature minimum of about 

S .5C. A "bubbLe" of water colder than 7C appeared to be 

separated trom the se?ward side of the cold core. The slope 

front, with the 10C isotherm contacting bottom at a depth of 

<85 m, was at a more normal shoreward position than in the 

pre vi o us section. 

Sec tion 7. Sea Education Ass~ciation RV ~~~1~2[Q' 16-17 May. 

Th is section, constructed from mechanicaL bathythermograph 

data , resembLed the previous one made five days earlier, although 

on t he shelf the minimum tem~erature in the cold core was about 

1C lower (4.2C) and the maximum in the warm Slope Water was 1C 

highe r (14.6C). Detachment of w2ter from the offshore side of 

the cold core appeared to be in progress. The elevation in 

bot t om temperature to 13C at depths below about 120 m, as well as 

the 14.SC water, indicated the presence of Gulf Stream warm core 

eda y 7 68 beyond the offshore end of the section (Fig. 19.2). 

Section 8 . WHOI RV ~QQ[r Cruise 58, 1-2 August. 

Surface temperatures, as well as the steepness and shallowness 

of the t h ermocLine, were at their observed annual maximums. Five 

sepa rate bodi~s of minimum te~perature water (colder than 9C) 

appea red in the cold core bottom water on the shelf, and a 

"bubb le" of 9.5-1 0 C water appeared to have "calved" from the 

offs hore side of the core. The slope front lay shoreward of the 

1GO - m isobath, as in the previous t~o sections, but had an 

u nus u a lly vertical configuration at depths below about 25 m. 

Se ction 9. WHOI RV Q£~£D~i Cruise 13-111, 12-13 August. 

This section apparently sho~ed cooling effects from hurricane 

Be lle, which crossed the shelf in a northward direction, with its 

center between 70wOO' and 70W3C·, three days before. Surface 

temperatures were 2-5C below those in the previous section, made 

a week before the hurricane; the thermocline was depressed about 

10 m, and the thickness of the cold core bottom water was reduced 

concommitantly. Temperatures in the cold core were more 

homogeneous than in the previous section, and the minimum was a 

de9ree warmerl but there was a similar "calved bubble" colder 

318 
than 10C near the offshore side of the core. ~arm core eddy 76C, 

located beyond the offshore limit of the section (Fig. 19.2) was 

presumed to have been the source of the isolated body of 13-14C 

water centered at about 90-m derth in the Slope ~ater zone. 

Inflections of isotherms were beneath this body. 

Section 18. wHO! RV ~QQ[[ Cruise 58-III, 27-28 August. 

Surface temperatures were warmer than in the previous section 

(section 9), made two weeks oefore, but remained about 2C cooler 

than in section 8, made prior to hurricane Belle. (In later 

sections, surface temperatures were also cooler than in 

section 8, except in section 12 made in early October.) The 

thermocline was nearer the surface than in section 9, but 

remained deeper than in section 8 and less sharply defined. Slow 

warming was apparent in the cold core water, which also had a 

"calving" tendency at its offshore margin. 

Section 11. WHOI RV Q£~2Q~~ Cruise 15, 18-19 September. 

Surface temperatures were about the same as in the previous 

section, made a month earlier, but were 2C warmer in the cold 

core bottom water, which had minimum temperatures >11C and was 

divided into two cells. The slope front had become thermally 

indistinguishable near bottom, because the cold core water had 

warmed to about the same temperature as the adjacent warm Slope 

Water (see Wright 1976). The domed feature in the upper 30 m at 

XBT stations 5-6 may be a cyclonic eddy from the slope front. 

Section 12. wHOI RV Q£~~Q~~ Cruise 15, h October. 

Surface temperatures at the shoreward end of the section were 

2C colder than over the same depths of water in section 11, made 

20 days earlier, and the onset of vertical mixing was apparent in 

the deepening of the surface layer. In contrast, surface 

temperatures, from about the 65- to 120-m isobaths, were warmer 

in section 12, with the difference increasing to about 1.7C in 

the offshore direction. This rise in temperature, in a season 

when cooling is normal and in a year when the air temperatures in 

October were abnormally low along the entire coast of the United 

States (see Chamberlin and Armstrong, Paper 11), presumably 

rerresents an influx of warm Slope ~ater. The prominent domed 

fe?ture in the upper 150 ~ at X9T stations 317-318 may be a 

cyclonic slope front eddy. If so, warm Slope water may have 

reached the shelf, near the surface, by entrainment around this 

feature. Influx of warm Slope Water to the shelf was also 

indicated below the subsurface by the rise in bottom temperatures 

to above 13C at depths around 70-80 m. At the bottom at 50-60 m, 

temperatures were about 15.5C, which was 3.5C warmer than in the 

previous section and ~as the ~aximum observed during the year. 

Section 13. NOAA RV ~lQ§l[Q~~ l~ Cruise 76-C~, 23-24 October . As a result of continued autu~n cooling, the Shelf Water was 

4-5C colder than in section 12, ~ade two weeks earlier, and 

319 
I

aper 11 

vertically mixed to a depth of 50 m. In the warm Slope Water at 

the offshore end of the section, vertical mixing was also evident 

to a depth of 50 m, and surface temperatures were colder by 3-5C. 

The few degrees rise of Slo~e Water temperatures in the 

50- to 100-m depth range off the shelf also may have been the 

result of tne vertical mixing. The zone of minimum temperature 

bottom water {colder than 13C), at depths of 80-100 m, was a 

degree colder than in the previous section. This temperature 

decline, if not a data artifact, may have resulted from advection 

of colder water from the east or west, or from upwelling of Slope 

Water, as indicated by the steep slopps of the 9-15C isotherms 

near bottom at depths below 120 m. 

Section 14. NOAA RV ~iQ2trQ~~ l~ Cruise 76-09, Y November. 

The verticaLly mixed Shelf Water, 2-3C cooler than in the 

previous section, had become colder than the underlying Slope 

Water, beyond the 60-m isobath. Within this underLying Slop e 

Water, the ~inimum tem~erat~re ~ater Lay on the bottom «13C at 

105 m depth), as in the previous section, but was greatly 

diminished in cross sectional area. Temperature elevation in the 

warm SLope Water area beyond the sheLf break and the deepening of 

isotherms at the bottom in depths below 120 m presumably 

refLected the presence of warm core eddy 76D, centered beyond the 

offshore end af the section (Fig. 19.2). 

Section 15. NOAA RV ~~~~~[£h~r Cruise 11-76, 27-28 November. 

Details in this section were uncertain because of the wide 

spacing between XDT stations. The vertically mixed Shelf Water 

was about 3C coLder than in the previous section made 18 days 

before. Temperatures in the underLying SLope Water were also 

cooLer by about 2C, but this water penetrated farther onto the 

shelf, extending some unmeasured distance shoreward of the 50-m 

isobath. Within the warm Slope Water on the outer shelf, the 

core of minimum temperature that was seen at the bottom in the 

previous two sections apparently no lonyer existed. Maximum 

temperatures ;n the Slope ~ater, warmer than 16C to a depth of 

75 m, were 2C cooLer than in the previous section, but still 

apparently reflected the presence of eddy 76D beyond the offshore 

lim i t of the s-e c t ion (F i g. 1 9 .2) • 

Section 16. WHOI RV ~DQrr Cruise 62, 21 December. 

The Shelf Water temperatures were only 1.S-2C colder than in 

the previous section made three weeks before, presumably because 

of relatively mild air temperatures along the Atlantic coast 

during December (see Chamberlin and Armstrong, Paper 11). 

Nevertheless, these water temperatures, being colder than at the 

same ti~e in December of the previous two years (Chamberlin 

1978), did seem to reflect the unusually cold air temperature 

th2t prevai led along the coast during fall 1976, especially in 

October and November (see Chamberlin and Armstrong, Paper 11). 

For example, bottom temperatures shoreward of the Slope Front in 

320 
section 16 averaged about 3.SC colder than in 1974, and about 

2.5C colder than in 1975. The intrusive Slope Water that 

occupied the bottom on the outer shelf was more withdrawn than in 

the previous four sections, but isolated remnants of 9C water 

emained, one of which contacted bottom at around 65-m depth. An 

apparently isolated body of 13-14C water also rested on the 

bottom at depths of 85-135 m, and may have been formed by counter 

eddying effects of warm core eddy 76D. Satellite imagery showed 

this eddy to have moved westward entirely beyond the section line 

at the time the section was ~ade.4 At the offshore end of the 

section, the steep thermal front in the upper 120 m of the water 

column suggested the inshore edge of a warm core eddy, but the 

satellite ima~e of one day later did not show an eddy but 

apparently onLy a large patch of warm Slope Water centered beyond 

the offshore end of the section. 

BOTTOM TEMPERATURES IN 1976 

The seasonal bottom temperature cycle in the waters south of New 

England is most pronounced in the Shelf Water region, shoreward 

of the zone where Slope Water contacts bottom (Colton and Stodard 1973; Wright 1976). A general chronology and description of 

the seasonal Shelf Water cycle for thi s region is giv~n by 

Bigelow (1933). 

During 1976, the observed minimum bottow temperature wa s 2.5C, at 

about 30-m depth in early February. Although temperature 

observations from as shallow as 30 m were lacking for February 

1974 and 1975, the bottom t~mperature diagrams for those years 

(Chamberlin 1978) indicated that the ninimums were about the same 

as in February 1976. In March 1976, however, the bottom 

temperature at depths around 30 m rose above 4C, whereas in 

mid-March 1975 it was below 3C and in March 1974 was probably 

below 3C. The early warming in 1976 was cunsistent with 

extremely warm air temperature conditions along the Atlantic 

coast in February (Dickson 1976). In depths of 40-50 m, the 

minimum observed bottom temperature ~as about 4C in March. This 

value is within the range described by Bigelow (1933). Beyond 

the 50-m isobath, cooling continued at the bottom into April as 

isotherms moved seaward to the JPper slope. The timing of this 

trend confor~ed closely to that in 1974 and 1975 (Chamberlin 

1978), although the recorded minimum was somewhat warmer. The 

minimum at 75-m depth, for example, was about 1C warmer than in 

-----

4EOFA (Experimental Ocean Frontal Analysis), 22 December. 

321 
t'd~t'r 17 

1974, and 2C warmer than in 1975. The extent and timing of this 

cooLing may be controlLed by movement of the Slope Front. 

However, the fact that the deepening of the isotherms on the 

outer shelf had occurred in April during each of the three years, 

sug~ested the alternative expLanation that the minimum SheLf 

Water temperatures of earLy spring promoted cross-frontaL mixing 

with the ~arm SLope Water. SaLinity data wi LL te necessary to 

determine whi~h explanation is correct. 

Shoreward of the 5G-m isobath, the bottom water began to warm by 

~id- Nar ch, risin g to about 7C (warmer inshore) before thermaL 

stratification set in by earLy ay, and estabLished this water as 

an iso Lated coLd core. ALthough data were were not obtained 

during June and JuLy, it appeared that summer temperatures in the 

co Ld core were si~ilar to those in 1Q74, but about 1C warmer than 

in 19(5. 

The ~dssaoe of hurricane He lLe across the shelf on 9-10 August, 

with its centpr about 1 0 nm (1 85 km) west of where data ~ere 

coLlected for this analysis, ~as apparent Ly Quite influential in 

cooLinn and deepenin~ the surface layer south of New EngLand (see 

diSCuss ion of section 9) , but had no 0 vious effect on botto~ 

tempera tures as seen in the s~ctions. 

CooLinq of the surface layer and verticaL mixing broke down the 

coLd core near the end of September, about a month earLier than 

in the prevlous two years. As a resuLt, midshelf bottom 

teffiperatures at depths around 75 m reachea the observed annual 

maximum (14-15C) by early October, which is aLso a month earlier 

than in 1974 and 197). The maximum values were similar, however, 

i~ alL three years. 

FoLLowi ng an incursion of SLope Water toward the end of October, 

which interr~pted the seaso~aL progression , SheLf Water cooLing 

at the bottom was rapid to a deoth of 75 m, and by the end of the 

year reachec vdlues, at that Lower depth, about 4C Lower than in 

1974 and 1975. The early breakdown of stratification and strong 

coolina pres~mably resuLted from unusuaLLy cold atmospheric 

conditions during October and November foLLowing beLo~ normaL air 

temperatures during the summer (see ChamberLin and Armstrong, 

P-3 ... er 11), 

The SLope Water, a band Lying between the SheLf Water and the 

Gulf Stream and having intermediate temperature values, is 

separatpd fro~ the Shelf Water by a thermal gradient that Wright 

(1976), in an anaLysis of historical data from 1941 to 1972, 

found to have an average midpoint temperature of 10C in the 

region south of New England, except for a brief period foLlowing 

the falL overturn when the minimum temperature Shelf Water is 

322 
frequently warmer than 10C. 

Aright also calculated an annual mean of 13.2C and a mean annual 

range from 12.3C to 14.6C for the maximum temperatures in the 

arm Slope Water that normally underlies the Shelf Water near the 

Duter shelf. Although nonseasonal events, such as incursions of 

ulf Stream Water or upwelling of deep Slope Water, may often 

~a sk ' seasonaL events in the Slope water near the bottom on the 

o uter shelf, it is apparent, nevertheless, that the warmest part 

of the warm Slope Water does not ordinarily contact bottom on the 

outer continental shelf. During 1974-76, for example, the 

maximum bottom temperatures were between 12.0C and 13.0C the 

great majority of the time (see also Chamberlin 1978). Furthermore, the maximum long-term monthly mean bottom temperatures on 

the outer shelf for the years 194C-66 were between 10.0C and 12C 

the great majority of the time (Colton and Stoddard 1973; 

Chamberlin 1978). Part of the reason that Colton and Stoddard's 

mean values are colder than the 1974-76 temperatures for the same 

de~t~ zone is that they were partly based on data from years when 

intrusion of cold Labrador Coastal Water displaced the Slope 

Water from the bottom south of New England (Colton 1968). This 

water is not evident in any of the temperature sections from 1974 

to 1976. 

wriqht (1976), in his analysis of historical data, also found 

that the slope front intersected the bottom at depths between 80 

and 120 m off southern New En~land 84% of the time. Beardsley 

and Fla gg (1976) suggested four possibl e mechanisms which might 

account for frontal movements: 1) propagation of barotropic 

waves, 2) baroclinic instabilities across the fron t , 3) local 

wind field variability, and 4) passage of Gulf Stream eddies. 

Frontal distortions caused by the first two mechanisms are 

assumed to be frequent and minor, but are not easily assessed by 

direct observation. The effects of wind stress transport, 

however, are known to be significant, although usually of brief 

duration (Boicourt and Hacker 1976). Passages of Gulf Stream 

eddies, although not frequent, may also cause significant 

variation in the slope front position by injection of Gulf Stream 

derived water, Slope Water displacement, and offshore entrainment 

of Shelf Water, accompanied by compensatory subsurface inshore 

flow of Slope Water (Chamberlin 1976; Morgan and Bishop 1977). 

During 1976, the maximum observed bottom temperatures in the warm 

Slppe Water zone ranged from slightly >12.0C to nearly 15.0C. 

This range is similar to that observed in 1974, but cooler than 

in 19/5, when unusually W3r~, as well as moderately colder, 

temperatures occurred. The observed inter- section of the slope 

front with the bottom was generally at derths shallower than 

1']0 m, except in April w'hen the depth was nearly 120 m, during 

the time when the Shelf Nater was at its annual minimum 

temperature in depths >70 m as described above. 

323 
Paper 1

1 

During 1976, dS in 1974, no data we re obtained to indic a te that 

bottom temperatures in the warm Lope ~ater zonp feLL bpLow 12C , 

as they did on at least t~o ~cc~sions in 197~. he parent 

absence of a minimum temperature intervaL ln arch ~ partic -

Larly interesting, becauce such an event occurreo in 1)75 and was 

stronoLy evident in Long-ter~ ~on hL) mean bo om empe r urps 

for the years 194u-66 (ChamberLin 1973). The dppare t absence of 

such a minimum in March 1~74 can be expLain d y the persistence 

of a warm core Gulf st ream eddy c:outh of ~e w England du ri 9 a 

month (ChamberLin 1976). In 197, howeve r, 0 warm ed y was 

detected in that re ~ion durin the en ir Wln er no e rly 

sprina. It seems possibLe, aLthou h questionabLe, hat hot 0 

temperatures at such a de th as the warm lo~e wa pr 

remained above 12C during 13rch 1975 ecause of he record war 

air temperature durina the precedina month ( ic son 976) . 

Two strong in~ursions of SLo e Water ~nto e up er slo e and 

outer shelf are evident: thp first in earLy Fe ruary and the 

other in Oc tober; but only the l tter a Pdrs to h~ve caused 

shoreward dispLacement of he sLor.e front (spp isclJss;on o f 

s ections 2 and 13). 

Bottom temperature variations can be ass o ciated with eac of the 

three Gulf St ream warm core eddies hat assed sou h of e w 

England during 1976 (Fig. 19.2). During ay, e dy 7 B p r esumab Ly 

caused the observed eLevation of bottom em era ures to above 13C 

in the warm Slope Water zone. Du rin mid-August , the p r esence of 

eddy 76C was probably refLected in the dee enin of isotherms (as 

much as 80 m) at depths below 15 0 Another etfect of this eddy 

may have been a temporary ris e in botto temr,era ure to above 13C 

in the warm zone, as suagested by dashed Lines in Fi ure 19.2. 

The occurren~e of such a botto~ temperature rise is indicated i 

sections 9 and 10, aLthough not actuaLly shown in eithe r 

sections. In Novembe r, eddy 76D prob~bLy causea the obse rve a 

rise in bottom temperatures to above 14C (probabLy above 15C) i 

the warm zone. The deepening Jf isotherms at dep th s belo 160 m 

may also have been caused by this eddy . 

S U Mr~ AR Y 

Shelf water temperatures durina the spring, particuLarLy as 

observed at the bottom, were about 1C warmer than in 1974 and 

about 2C warmer tnan in 1975, r robabLy as a resuLt of record warm 

air temperatures in February and moderate air teMperatures in the 

following few months. 

~arked cooLing and deepening of the surface Layer was recorded on 

the shelf folLowing the passage ~f hurricane BeLLe in early 

August. 

324 
he cold core bottom water warmed to the level of the adjacent 

warm Slope ~ater by the end of September, about a month earlier 

than in 1974 and 1975. 

~t the end of the year, followin~ record cold weather in the 

fall, the Sbelf Water was 3-4C colder than in the previous t~o 

years. 

aximum bottom temperatures in the warm Slope Water zone on the 

outer shelf were not recorded below 12C nor above 14C during the 

year. 

Three Gulf Stream warm core eddies apparently passed 

England during 1976 (the same number as in 1974 and 

the first two, in late spring and late summer, 

developed and their influence on bottom temperatures 

ACKNOWLEDGMENTS 

south of New 

in 1975) but 

were weakly 

moderate. 

Several scientists kindly supplied the data for the temperature 

sections: Robert C. Beardsley, Woods Hole Oceanographic Institution (WHOI), sections 1, 2, and 9; Bradford Butman, U.S. 

GeologicaL Survey, Woods Hole, MA, section 6; Steven K. Cook, 

Atlantic Environmental Group (AEG), N~FS, sections 8, 10, 11, and 

12; William G. ~etcalf, WHOI, section 16; Henry Jensen, Samuel 

R. Nickerson, and W. Redwood wright, Northeast Fisheries Center, 

Woods Hole, MA, sections 3, 4, 5, 7, 13, 14, and 15. Reed 

S. Armstrong, AEG, gave his usual valuabLe advice. 

LITERATURE CITED 

BEARDSLEY, R. C., and C. N. FLAGG. 

1976. The water structure, mean currents, and sheLf-waterl 

slope-water front on the New England continental shelf. 

Mem. Soc. R. Sci. Liege (Ser. 6) 1C:209-225. 

BIGELOw, H. B. 

1933. Stuuies on waters on the continental shelf, Cape Cod to 

Chesapeake Bay. I. The cycle of temperature. Mass. Inst. 

Technol. and Woods Hole Oceanogr. Inst. Pap. Phys. Oceanogr. 

Meteorol. 2(4), 135 r. 

BOICOURT, W. c., and P. W. HACKER. 

1976. Circulation on the Atlantic continental shelf of the 

United States, Cape May. to Cape ~atteras. Mem. Soc. R. Sci. 

Liege (Ser. 6) 10:187-200. 

325 
C H A IV. a E: f.\ LIN , J. L. 

1976. 80tiom temper~ture conditions on the continentaL sheLf 

and slope south of New Eng Land during 1974. 1D J. R. 

GouLet, Jr. (com~iLer), T e environment of the United States 

Living marine resources - 1974, • 1 -1--18-7. U.S. Dep. 

Cammer., NatL. Oceanic Atmos. Admin., NatL. Mar. Fish. 

Serv., ~AR~AP (~ar. Resour. Monit. Asses. redict. Progra ) 

Contrib. 104. 

1Y7o. Temperature structure on the continentaL s Lf and 

slo~e s0uth of New England durin 975. 1Q J. R. Goulet, 

Jr. and E. D. haynes (editors), Oce n variabiLity: Eff cts 

on U.S. marine fishery resources - 1975, 271-292 . u.s. Dep. COIWter., NOAA Tech. Rer. MFS Circ . 416. 

COLTON, J. 8., Jr. 

1<760. Fecent tr nds ln 

~aine end contlquous 

25 : 2427 -2. 437 • 

su surface tem eratures in he G Lf of 

watprs. J. Fish. Res . Board Can. 

COLTON, J. B., Jr. and P. • STODDA D. 

1973. &ottom-water tern eratures on the 

Novi'l Scotia to ~Iew Jers y. U.S. Dep. 

Rep. NMF~ CIRC-376, 55 r. 

DICKsor, R. R. 

co tinenta sheLf , 

Co mer., 0 A Tech . 

1976. weather and circuLation of Fehruary 1 6. Extre e 

warmtr over the eastern two-thirdS of t e United States. 

Mo. ~eather Rev. 104:660-665. 

MORGAN, C.h., and J. ~. bISHOP. 

1977. An p.xarrpLe of GuLf Stream eddy-induced water exchange 

in the mid-AtLantic Bisht. J. Phys. Oceanoor . 7:472-479. 

TAU8ENSEE, R. E. 

1 976. l'l e at her and c i r c u L 2 t ion 0 f 

precipitation around the Great 

104: 8(' 9-814. 

WRIGHT, w.R. 

arch 1 76. 

Lakes. 

Record heavy 

o. weather Rev. 

1976. The Limits of sheLf water sJuth of Ca~e Cod, 

1972. J. tw'lar. Res. 34:1-14. 

1941 

326 
71 0 301 

D P 1 

1 

1 

1 

1 

1 

1 

------- -----~------------. 

------------.--- 1 

1 

1 

1 

1 

1 

i 

1 

1 

1 

1 

1 

1 

1 

1 

1 

' .. ' . ... 1 

~4!~-------0"-~-----~--------------------~----- 1 I 1 ~e!0' . .. .. : : 

"~ , ~.,-~ 1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

.---------r-------------------1------

1 

1 

1 

16 1 --------------------r----- 1 

1 . • 

-------~-----~.:. .;:..------- 6 1 • 1 •• • 

I · 

... 200 fl · . : • 1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

12 

Figure 19.I.-Locations of vertical temperature sections included in this report. Sections are numbered chronologically. See Appendix 19.1 for 

identificatio n of sections_ 

327 
MONTH 

J 

o 

(J) 100 

a:: 

UJ 

.... 

UJ 

~ 

I 

/ 

:J: / 

.... / 

a. 200 

UJ I 

0 / 

/ I 

I 

::E I 

/ 

0 / 

.... I 

l- I 

0 

CD 300 

~8~ !S§> 6°C 

/ " ~< 12°C 

J -- --7- - -- .. 400 

1-----1 t--; > 

768 76C 76 D 

Figure 19.2.-Bottom temperatures on the continental shelf and slope south of New England during 1976. Temperature sections are numbered 

along the top margin (see Appendix 19.1). Dots mark the depth limits of the bottom data from each section. Horizontal lines at the bottom of the 

diagram indicate the times of Gulf Stream anticyclonic eddy passages south of New England. 

328 
Section 

APPENDIX 19.1 

Vertical temperature sections of the continental shelf and slope regions south of New 

EngLand during 1976. Solid line isotherms 

ore at 1C intervals. The dashed line isothe(ms, which appear occasionally, are at 

C.5C intervals. Hatched areas represent isot her mal wa t e r. 

1.--NOAA PV 1$~.1~~ Cruise 76-01, 4 February. 

Section 2.--t\JOAA RV ~~l~~ Cruise 76-G2, 9-10 February. 

Section 3.--NOAA RV ~.1Q21r:Q~~ I~ Cruise 76-01, 23-24 February. 

Section 4.--N OAA RV ~1~21r:~~~ l~ Cruise 76-02, 25-26 March. 

Section 5.--Polish RV ~i~£~QQ Cruise 76-01, 10-11 April. 

Section 6.--Duke Univ. RV ~§~1~2r:Q Cruise E2876, 11-12 May. 

Section 7.--Sea Educ. Ass'n. RV ~~~!~2r:Q Cruise of 16-17 May. 

Section 8.--WHOI RV ~U~r:r: cruise 58, 1-2 August. 

Section 9.--WHOI RV Q£~2D~~ Cruise 13-111, 12-13 August. 

section 10.--WHOI RV ~U~r:r: cruise 58-III, 27-28 August. 

Section 11.--WHOI RV Q£~§D~~ Cruise 15, 18-19 September. 

Section 12.--wHOI RV Q£~§u~~ Cruise 15, 8 October. 

Section 13.--NOAA RV A1Q21r:Q~~ I~ Cruise 76-09, 23-24 October. 

Section 14.--NOAA RV Al~21r:~~~ l~ Cruise 76-09, 9 November. 

Section 15.--NOAA RV R~~~§r:£h~r: Cruise 11-76, 27-2b November. 

Section 16.--WhOI RV ~u~r:r Cruise 62, 21 December. 

329 
SECTION I 

in I 5 

x 

o -r+-.-r'--+r1--,............, 

50 

0 30 

NAUTICAL MILES 

SECTIO J 3 

~ 102 104 11

CD 

SECTION 2 x 

0 ~ 5 

CD 7 9 18 

x 

0 

50 

50 

100 

(J) 

c::: 

W 100 

t- 150 

W 

~ 150 

200 

I 

ta... 200 

W 250 

0 

250 FEB 23-24 

300 

0 50 

300 

NAUTICAL MILES 

350 

FEB 9-10 

400 

0 50 

NAUTICAL MILES 

330 
,... 

'f) 

t: 

:L.I 

.u 

J 

D 

fCD 

SECTION 4 

x 201 202 208 210 

o ~~~--~~~~--~~~ 

50 

100 

150 

200 12 

250 

300 

0 50 

NAUTICAL MILES 

SECTION 5 

2 4 6 9 10 

0 

50 

100 

150 APR 10 - II 

0 50 

NAUTICAL MILES 

fSECT ION 6 

CD 

x 2 14 

0 

50 

100 

150 

200 

250 

300 

350 

400 

MAY 11-12 6 

0 50 

NAUTICAL MILES 

331 
..... SECTION 7 ~ 4A IA 

0 12 

50 

100 

(/) 

0:: 150 

W 0 50 

r NAUTI CAL MILES 

w 

~ 

I 

..... S EGTION 8 

r ~ I 5 

a.. 

0 

W 

0 

50 

100 

150 

50 

N AUT I CAL MILE S 

..... 

ro 

x 2 

0 

50 

100 

150 

200 

250 

300 

350 

0 

..... 

ro 

xl 

50 

o 

SECTION 9 

4 6 8 10 12 14 1618 

AUG 12-13 

50 

NAUTICAL MILES 

SECTION 10 

50 

NAUTICAL MILES 

9 

-21 

3Z2_~~~ ______ ~ __ 

~ 

CD 

x 201 

SECTION 13 

208 215 

O~------~~~~~~I 

-

Cf) 

~ 

w 

r 

50 

100 

w 150 

~ 

"-'" 

I 

r 

CL 

W 

o 

300 

350 

o 50 

NAUTICAL MILES 

~ 

CD 

SECTION 14 

x 305 313 

o 

50 

100 

150 

300 

350 

NOV 9 

o 50 

NAUTICAL MILES 
~ 

SECTION 16 

~ 312 304 301 

0 

SECTION 15 ~ 

OJ 

x 4 6 7 9 50 

0 

100 

50 

150 

U) 

0::: 100 

W 

IW 200 

~ 150 

I 250 

I- 200 

0... 

W 

0 10- 300 

250 

350 

300 

0 50 400 

NAUTICAL MILES 7 

DEC 21 

450 

0 50 

NAUTICAL MILES 

335 . 
Paper 20 

CONTINUOUS PLANKTON RECORDS: ZOOPLANKTON AND 

NET PHYTOPLANKTON IN THE MID-ATLANTIC BIGHT, 1976 

Daniel E. Smith and Jack W. Jossi l 

The seasonal abundance and variation of zoopLankton and net 

phytopLankton at a 10-m depth, in the Shelf and SLope Waters of 

the New York and Chesapeake Bights, were assessed by Continuous 

PLankton Recorders (CPR) (Hardy 1939). U.s. Coast Guard cutters 

and research vessels towed the CPR's between the mouth of 

Chesapeake Bay and Ocean Weather Station HOTEL (38N, 71W), and 

between Ambrose Light, New York Harbor, and Deep Water 

Dumpsite 106, as part of a cooperative agreement between the 

MARMAP Progra~ of the NationaL Marine Fisheries Service and 

(1) the u.S. Coast Guard for the at-sea collecting of data and 

(2) the Institute for Marine EnvironmentaL Research (IMER) of the 

United Kingdom for a southern extension of the Long-term survey 

of pLankton dynamics in the North AtLantic by which IMER has been 

monitoring seasonaL and long-term changes since 1930. The 

zoopLankton of a warm core GuLf Stream eddy which passed through 

the survey area are also described. 

SEASONAL ABUNDANCE AND VARIATIONS OF 

ZOOPLANKTON A~D NET PHYTOPLANKTON 

The CPR routes are shown in Figure 20.1. Shelf Water 

data for the New York and Chesapeake Bights are 

Figures 20.2, 20.4, and 20.6. SLo~e Water plankton 

these areas are shown in Figures 20.3, 20.5, and 20.7. 

pLankton 

shown in 

data for 

Because a major objective of these 

Long-term cyees, means, and trends, 

present the data on an annual basis 

detailed anaLysis is feasible. As 

surveys is to describe 

it was felt appropriate to 

rather than wait untiL 

a resuLt, the data are 

IMARMAP Field Group, Natio~al Marine Fisheries Service, NOAA, 

Narragnasett, RI 02882. Present address: Atlantic Environmental 

Group, National Marine Fisheries Service, NOAA, Narragansett, RI 

02882. 

3 
Paper 2(; 

presented itn little ca~ment. Po w~ver, some expLanation of the 

units resented and the countin~ system which produced them is in 

order. The counting system used was designee to allow for the 

raoid dnaLysis of large numbers of plankton samples taken month l y 

from large orc:as of the ":Jrth AtlanTic Ocean. 

Phyto~Lankton were recorded as number of occurrences per twenty 

O.295-m~ di?weter microscopic fields t2ken diagonaLly across a 

section of boLting silk ",hich had fiLtered 3 01 of seawater (a 

10-n mi Sample). The silk aoe rture size was 225 x 234 mm. Mean 

occurrences of each taxum per w~ter mRSS per month are shown in 

F,aures 20.2 and 20.3. 

Zoo lankton were counted by either of two methods, oepending on 

their size. Zooplankton taxa <2 mm seen in a staggered traverse 

of thp si lk were estimated to falL within one of a set of 

abunda ce categories. An "acce~ted vaLue" (!.JeighTed mean) was 

sucstituted fJr each cate90ry, and these accepted values were 

multi Lied by an aliquot fector to g ive the number of plankton 

per samrLe (3 cu m). FinaLLy , the numbers for all anaLyzea 

sampLes per !.Jater mass ~er month (see Fig. 20.1) were averaged 

together to optain the numbers shown in Fi~ures 20.4 and 2G.5 . 

Zooplankton >2 mm ~ere anaLyzed in the some manner except that 

the number of aLL animaLs :In a silk was recorded, thereby 

precl ding the need for an ali~uot factor. These data are shown 

in Figures 20_6 and 20.7. For mo r e detai Ls concerning these 

methods see CoLebrook (1960) . Some taxa of zooplankton were 

present in both size categories (usuaLly d ifferent deveLopmenta l 

staqes) and are presented separately . 

TwO fedtur~s of the plankton dynamics which are not obvious fro~ 

the figures are mentioned bel:Jl.i. Thecosorn ate p teropods increased 

and d crEased aLono with the ~~ [£ti~m t[i~Q~ bloom in all 

instances durlng the springtime . Co~pare Figures 2Q.2 with 20.4, 

anu 20.3 ~ith 2G.S. The cLauJce ran E~QQili§ SPa dominated the 

plan ton in October Chesa~eake Bight She lf Water sa~ple$ in 1976 

ut were not abundant in fall sampLes of 1974 and 1975. 

lOOPLANKTO' )F A WAR~ CORE ~DDY 

d CdY d w rm c re GuLf Str am 

~.S. vy ceano_ra hic Office) 

F ru ry 1976 (Fi . 2G .1). 

vironmen al Group , , rr q ns tt , I ,...., 

J. 

eddy (called Eddy 0 by the 

was traversed by the CPR in 

ationa l 

8 . Un uhl . 

~arine 

datd . 

Fisheries 
Paper 20 

inated the zooplankton within the eddy but also were more 

numerous withjn thp eddy than without. ALL other taxa of 

plankton were more numerous in SheLf and Slore water sampLes than 

in the eddy samples. The history of this eddy and the 

distribution and abundance of these copepod species show some 

interesting relationships. 

Gotthardt (1973) showed that warm core Gulf Stream eddies form 

from GuLf Stream meanders, ~hich break off into the Slope Water 

forming a GuLf Stream Wat~r ring surrounding a Sargasso Sea Water 

core. A GuLf Stream meander was shown southeast of Georges Bank 

on the 25 June 1975 Experimental Ocean Frontal Analysis (EOFA) 3 

chart. A week later the 3 0 June chart indicated a feature which 

was later shown to be Eddy D. 

Th~ Gulf Stream and a small area of the Sargasso Sea east of the 

Chesa~eake 8ight were sampLed in June 1975. No M. l~£~nl was 

found, which is consistent with the findings of other 

invfstig?tcrs in this area. It can be assumed t~at Eddy D formed 

without ~ny ~. t~£~Gl. Although t. ~[~£itil was not found in any 

summertime, 10-m CPR samples of the Gulf Stream, Bowman (1971) 

found it abundant in all seasons in GuLf Stream sampLes taken 

between ttle surface and 70 m. ~l~~[~m~mm§ ~[~£ilil may have been 

~resent in the deep water of the eddy. 

Tre EOFA char~s showed Eddy D moving westw ard from southeast of 

of Georqes 8ank in Late June 1975 to the New York Bight area in 

Decewoer ~975. It appeared from the charts to be entra i ning 

SLope and SheLf Waters as it ~ent. ~~lIi~i~ l~£~QI appeared in 

Chesapeake Bight SheLf Water sampLes in November and December 

1975 and S lope ~ater samples in December 1975. El~Y[Qm§mm~ 

g[§~i~il appeared in both Shelf and Slope Waters in November and 

Dece~oer. It is likely that these two species also occurred in 

SLope Water in the vicinity of Eddy D. Eday D may have been 

colonized by ~. l~£~Q~ from the Shelf and Slope Waters which it 

entrained to the south of New England. 

During January 1976 every SLope Water sample from the New York 

Bight contained E. ut~~itil and ~. t~£~nl' while SheLf Water 

samples aLso contained ~. lY~~D~. It can be assumed that Eddy D 

entrained so~e of these as it waved throu ph the New York Sight 

SLope water. 

3U.S. Navy Oceanographic Office, Applications Research Division, 

Suitland, ~D 20374. 
t-

dfJer .::u 

Oy January and nhruary 1~76, ~drly D had mo v ed sout hw estwa rd from 

the !'lew York o;,'ht tn the ~o itions shown in Fig re 20 .1. 

However, in the Chesapeake 8i~ht 

eddy, ~. l~f~n~ dnd • g!:!:!fili 

Slop Water samples , outsid~ 

ad beco absent by Januar . . 

In February, ~r n .ddy D arrived in thp Ch sapeake Biu t, 

contained more ~. l~£gO~ and C· 9(oki li than eit er Chesa~eakA bight shelf or S lope Water, and ~Ore han the ew 

dight Slope water thr ugh ~hlrh it had COle. Howeve r, t 

time the abundance of ~. l~£_o~ ~nd . r_~ili~ was also 

increasina in CLe5a~eake Eight Sh l nd lo~e a prs. 

It ;s postuLated: that Eddy 0 broke off from the Gulf tream 1n 

June 197~ containiny E. g[~£iti~ b t ro ~. l~£g_~; that Edd y 0 

was ~0puLated with l~£gQ~ from ent rained S plf and Slo~e 

Wa ters as it traveled to the est an southwest ; thdt • lV'~Qi 

and E. g!:!£ili~ re roduced more and/or survived longer in the 

eddy than they did in the S lo e or SheLf Water; and that it ;s 

unlikeLy that ~. L~£gQ~ accumu l~t ed in Edd y D by si pLe ad ition 

of recruits frcm outsi e the ed y , cecause if this were the 

reason for its abuncance, other ~heLf and SLo e Water species 

would be expected to have acc m~lated in the sa e manne r an this 

Has not tne case. 

CKiJ LE DG~E~ TS 

~e t~ank the ~taffs of the U. S . Coast Gua rd, AtLantic Area, 

~arine Services Divls;on; the u.s . Coast Gua rd Oc eanographic 

Unit; and the officers and cre~s of the Coast Guard cutters 

~l~tt, 2illii' Q~~Q~ ' ~~ll~t iQ' ~~l i~~Q£~' ana I!Q~t. Ie also 

thank the Sea Education Association , tne officers and crew of 

their RV ~~~~~!t~, ana the personneL of the NOAA ship Q[~g~Q II. 

Without the help of these groups , this su rvey woulc not have been 

fjossit: Le. 

340 
lITERATJRE CITED 

OWMAN, T. E . 

1971. The distribution of caLanoid cope pOdS off 

eastern United States bet~een Cape ~atteras 

FLorida. Smithson. Contrib. Zool. 96, 58 p. 

,OlEB OOK , J. 11':. 

1900. Continuous pL rkton records: methods 

195 -59. uLL . Mar. EcoL . 5 :51-64. 

OTTHARDT, G. A. 

the southand southern 

of analysis, 

1 3. uulf Stre m eddips in the western tlOrth Atlantic. U.S. 

ovy Ocean00r. Off., fJ.VOCEA.O Tech. Note 6150-16-73,42 p. 

ARDY, A. c. 

193. -co Lo 

Recorder: 

1:1-57. 

ical invest; 9a tions with the Continuous Plankton 

bject, pLan and methods. HuLL Bu ll. Mar. EcoL. 

341 
ST 

SL .,., .,., .,., .,., 

36· ~~--L- ~~--~--~--~ 

76° 

Figure 20. I.-Positions of water masses, surface fronts, and continuous plankton recorder samples during 1976. SH = Shelf Water, SL = 

Slope Water, ST = Gulf Stream Water, SS = Sargasso Sea Water, WE = warm eddy (after U.S. Navy Experimental Ocean Frontal 

Analysis 1976), - = 10-mi sample. 

342 
:30 

28 

26 

24 

22 

(f) 

o 20 

...J 

ILl 

I.L. 18 

o 

N 

...... 16 

ILl 

() 

Z 

ILl 

a: 

a: 

::l 

U 

U 

o 

14 

12 

10 

8 

6 

4 

2 

o-I-Fr:..:... 

NY BIGHT CHESAPEAKE BIGHT 

30 

MONTH 

* NO SAMPLE 

- BLUE -GREEN ALGAE 

DINOFLAGELLATES 

1

2 CERATIUM TRIPOS 

3 C FUSUS 

4 C MASSILIENSE 

5 OXYTOXUM SPP 

SILICOFLAGELLATES o 6 SILICOFLAGELLATES 

DIATOMS 

7 THALASSIOSIRA SPP 

8 BIDDULPHIA ALTERNANS 

9 THALASSIONEMA NITZSCHIOIDES 

10 NITZSCHIA SERIATA 

II RHIZOSOL ENTA ALATA FORMA AL.llA 

12 R ALATA FORMA GRACILLIMA 

13 R ALATA FORMA INDICA 

I~ R. HEBETATA FORMA SEWISPINA 

15 THALASSIOTHRIX LONGISSIMA 

16 CHAETOCEROS SPP 

17 COSCINOIlISCUS SPP 

18 CERATAULINA BERGONII 

19 ASTERIONELLA JAPONICA 

20 SKELETONEMA COSTATUM 

Figure 20.2.-Net phytoplankton abundance in Shelf Water of the New York and Chesapeake Bights, 1976. ee text for explanation of 

abundance units. 

343 
NY BIGHT 

20 

18 

(/) 

16 

0 

...J 

W 14 

u... 

0 12 N 

..... 

W 10 

U 

Z 

W 8 Q: 

Q: 

:::> 

U 6 

U 

0 

4 

2 

0 

_* NO SAMPLE 

BLUE -GREEN ALGAE 

OINOFLAGE LLATES 

2 CERATIUM TRIPOS 

3 C FUSUS 

4 C MASSILIE NSE 

!! OXYTOXUM SPP 

SILICOFLAGELLATES o 6 SILICOFLAGELLATES 

DIATOMS 

7 THALASSIOSIRA SPP 

B BIOOULPHIA ALTERNANS 

9 THALASSIONEMA NITZSCHIOIDES 

10 NITZ SCHIA SERIATA 

I I RHIZOSOLENTA ALATA FORMA ALATA 

12 ~ ALATA FORMA GRACILLIMA 

13 R ALATA FORMA ~ 

14 R HEBETATA FORMA SEMISPINA 

15 THALASSIOTHRIX LONGISSIMA 

16 CHAE TOCE ROS SPP 

17 COSCIN ODISCUS SPP 

IB CERATAULINA BERGONII 

19 ASTERIONELLA JAPONICA 

20 SKE L ETONEMA COSTATUM 

CHESAPEAKE BIGHT 

MONTH 

Figure 20.2.- Net phytoplankton abundance in Slope Water to the seaward of the ew York and Chesapeake Bights. 1976. 

See text for explanation of abundance units. 

344 
NY BIGHT 

4000 

3600 6 

7 

3200 .... 

2800 22 

." 

::IE 2400 

rtl 

..... 18 

a: 2000 

W 

CD .' . 6 

::IE 22 

:::> 1000 

Z 

1200 

800 

400 -::.: '18. '18 .... 

' .. :", .... 

0 

SON 

MONTH 

"* NO SAMPLE 

CJ THECOSOMATE PTEROPODS 

_ 2 LARVACEA 

OTHER CRUSTACEA 

§ :5 EUPHAUSID CALYPTOPIS 

CLADOCERA 

E3 4 PENN ILIA SPP 

E3 5 PODON SPP 

EURYTHERMAL COPEPODS 

D 6 PARACALANUS PSEUDOCALANUS SPP 

7 OITHONA SPP 

8 CLAUSOCALANUS SPP 

9 HARPACTICOID COPEPODS 

10 COPE POD NAUPLII 

TROPICAL - SU8TROPICAL COPEPODS 

I

II CORYCAE US SPP 

12 ONCAEA SPP 

13 CALANUS ' MINOR COPEPODITES 1-4 

14 EUCALANUS SPP COPEPODITES 1-4 

15 ACARTIA DANAE 

16 CENTROPAGES VELIFICATUS 

17 TEMORA TURBINATA 

COLD TEMPERATE COPEPODS 

[J.::. 18 CENTROPAGES TYPICUS 

.. ..::. 19 TEMORA LONGICORNIS 

: .::'. 20 PSEUDOCALANUS MINUTUS ADULTS 

.::. 21 CALANUS FINMARCHICUS COPEPODITES 

OTHER COPE PODS D 22 OTHER COPEPODS 

CHESAPEAKE BIGHT 

6 6 

.' . '18' 

:18.·.· .. * 

J F M 

Figure 20.4. -Zooplankton «2 mm) abundance per 3 m3 in Shelf Water of the New York and Chesapeake Bights, 1976. See text for explanation 

of abundance units. 

345 
1200 NY BIGHT 

1000 

.., 

:t 800 

rr> 

...... 

en 600 0: 

W 3 

CD 

~ 400 ::J 

Z 

22 

6 

7 

200 8 

:18 ' " . 

0 * ' 21 * 7 

M A M J J * 

MONTH 

NO SAMPLE 

I THECOSOMATE PTEROPODS 

2 LARVACEA 

OTHER CRUSTACEA 

§ 3 EUPHAUSID CALYPTOPIS 

CLADOCERA 

" PENNILIA SPP 

:I PODON SPP 

EURYTHERMAL COPEPODS O 6 PARACALANUS PSEUDOCALANUS SPP 

7 OITHONA SPP 

8 CLAUSOCALANUS SPP 

9 HARPACTICOID COPEPODS 

10 COPE POD NAUPLII 

TROPICAL - SU8TROPICAL COPEPODS 

I

II CORYCAEUS SPP 

12 ONCAEA SPP 

13 CALANUS MINOR COPEPODITES 1- 'I 

1'1 EUCALANUS SP!, COPEPODITES 1-'1 

IS ACARTIA DANAE 

16 CENTROPAGES VELIFICATUS 

17 TEMORA TURBINATA 

COLD TEMPERATE COPEPODS 

[J: 18 CENTROPAGES TYPICUS 

: .: .. 19 T EMORA LONGICORNIS 

. : ". 20 PSEUDOCALANUS hllNUTUS ADULTS 

•• :' . 21 CALANUS FINMARCHICUS COPEPODITES 

OTHER COPE PODS o 22 OTHE R COP EPODS 

CHESAPEAKE BIGHT 

Figure 20.5.-Zooplankton «mm) abundance per 3 m' in Slope Water to the seaward of the New York and Chesapeake Bights, 1976. See 

text for explanatiQn of abundance units. 

346 
NEW YORK BIGHT CHESAPEAKE BIGHT 

~o 

35 

30 

If) 25 E 

rt') 

"-

(f) 20 

a:: 

iLl 

m 

~ 15 

::::> 

Z 

10 

5 

0 

MONTH MONTH 

* NO SAMPLE 

~ I FISH LARVAE 

2 FISH EGGS 

3 CHAE TOGNATHS 

4 POLYCHAETE WORMS 

OTHER CRUSTACEA 

5 HYPERl1D AMPH IPODS 

6 DECAPODS 

7 DECAPOD LARVAE 

8 LUCIFER Spp, 

9 OSTRACODS 

10 EUPHAUSID 

II EUPHAUSID JUVENILES 

12 EU PHAUSID ADULTS 

COLD TEMPERATE COPE PODS 

r':': 113 METRIDIA LUCENS 

::'::: 14 CAL ANUS FINMARCHICUS 

EURYTHERMAL COPEPODS 

D 15 PLEUROMAMMA GRACILIS 

16 CANDACIA ARMATA 

TROPICAL - SUBTROPICAL COPE PODS 

1

17 LABIDOCERA AESTIVA 

~ EUCALANUS MONACHUS 

19 CALANUS MINOR 

20 EUCHIRELLA ROSTRATA 

21 EUCHAETA MARINA 

22 UNDINULA VULGARIS 

Figure 20.6.-Zooplankton (>2 mm) abundance per 3 m' in Shelf Water of the New York and Chesapeake Bights, 1976. See text for explanation 

of abundance units. 

347 
NY BIGHT 

CHESAPEAKE BIGHT 112 

45 

40 

35 

It) 30 

::E 

j() 

...... 25 

CJ) 

a:: 40 W 

CD 20 

::E 14 :) 

Z 

15 

10 

5 

0 

MONTH 

* NO SAMPLE 

~ I FISH LARVAE 

2 FISH EGGS 

3 CHAE TOGNATHS 

4 POLYCHAETE WORMS 

OTHE R CRUSTACEA 

5 HYPERIIO AMPHIPODS 

6 DECAPODS 

7 OECAPOD LARVAE 

8 LUCIFER Spp 

9 OSTRACODS 

10 EUPHAUSID 

II EUPHAUSID JUVENIL ES 

12 E U PHAUSID ADULTS 

COLD TEMPERATE COPE PODS 

m 13 METRIDIA LUCENS U 14 CAL ANUS FINMAFICHICUS 

EURYTHERMAL COPEPODS 

D 15 PLEUROMAMMA GRACILIS 

16 CANDACIA ARMATA 

TROPICAL - SU8TROPICAL COPEPODS 

~ 17 kABIOOCERA AESTIVA 

~ EUCALANUS MONACHUS 

~ 19 CALANUS MINOR 

~ 20 EUCHIRELLA ROSTRATA 

21 EUCHAETA MARINA 

22 UNDINI.lLA VULGARIS 

Figure 20.7.-Zooplankton (>2 mm) abundance per 3 m' in Slope Water to the seaward of tbe • ew York and Cbe apeake Bight. 1976. ee text 

for explanation of abundance units. 

348 
Paper 21 

SIPHONOPHORE ("LIPO") S\JARMING II~ NEW ENGLAND 

COASTAL WATERS--UPDATE, 1976 

Carolyn ~. Rogersi 

The Northeast Fisheries Center has continued to examine the 

distribution of ~~Q~mil £A£A. During the winter of 1975-76 there 

were few reports of net-clogsing organisms. In Late March and 

April reports from Gloucester, MA, indicated that fishermen again 

were encountering tllipo." 

Port agents a~ked interested fishermen to bring in sampLes of 

"lipo" and othp.r net-cLogging organisms for examination. Several 

fishermen fron Gloucester anc Portland, ME, colLected samples. 

Similar organisms were collected from ~~~Qt[~~~ l~ trawl nets 

during fishery resource assessment surveys in New England coastal 

waters. In addition, sam~les of plankton, neuston, and bottom 

sediments were collected from Cape Ann to the wilkinson Basin and 

in the Scantum Basin area from the ~l~~!rQ~~ I~ in A~ril and 

again in May (Fig. 21.1). 

Examination of bottom samples which were collected with a variety 

of gear (naturalists' dredge, Dietz-Lafond grab, Ponar grab, 

S mit h - r~ c I n t y reg r a b ) 2 rev e ale d n 0 lip 0 l ike 0 r 9 d n ism s • P l a n k ton 

and neuston samples collected on the April cruise had 

siphonophores at all locations, but they ~ere not abundant. 

Concentrations of Eh£~Q£Y~li~ Q~~£h~lii' a planktonic alga which 

is enveloped in large gelatinous masses in the spring during its 

reproductive phase, were also found in these samples, with 

greatest densities in the more coastal (shallo~) locations oft 

Cape Ann and Newburyport, MA. 

During May, ~. £![j was present in the plankton. However, as in 

April, numbers were low along the entir~ transect. In addition, 

the siphonophore colonies were smaller than those collected in 

autumn 1975. During our earlier studies (Rogers 1978), three 

iNortheast Fisheries Center, National Marine Fisheries Service, 

NOAA, Narragansett, RI Q288l. 

2Reference to trade names does not imply endorsement by th~ 

National Marine Fisher;~s Service, NO~A. 

349 
categorie5 of relative abundance were establi5hed based on the 

number of siphono~hore remains in the pLankton samples: high, 

moderate, ana few. ALL samples in spring 1976 were categorized 

3S "few" com~ared to the autumn 1975-winter 1976 estimates which 

were generaLly "high." 

Examination of samples obtained from trawL nets during April 

revealed the usual invertebrates, such as brittLe stars, worms 

and worm tUbeS, bryozoans, hydroids, sma ll bivaLves, urchins, and 

Large jellyfish. The principa l sources of gelatinous material in 

these sam~les, however, were ~~riQDth~~ QQr~gli~ tubes. 

~f[i~Dlb~~ ~Q[~~li~ is an anemonelike antbozoan which constructs 

a long, rough, thick tube of mud and various other materials 

cemented together by mucus. The tubes are often 2 feet in Length 

and are turiell in sandy bottoms. ~f[i§Dl.b ~~ QQ[f~li~ is a very 

abundant s~~cies throughout the Gulf of Maine and especially in 

deep water. In addition, two samples contained Eh~fQ£ ~~ti~; one 

was from an inshore location and the other, which also contained 

si~hono~hore~1 w?s collected in the Fip~enies area. In general 

aLL the samples examined contained the typical numbers and 

species of orJanisms which would be expected at this time of year 

3t the locations sampLed. 

Conversations with porl agents from Pt. Juaith, RI, and New 

Bedford, ~rovinc~town, and Bo ston, MA, indicated that there haa 

been no ~;gnificant problem with net-fouling organisms on vessels 

fishing from these ports during spring. Port agents Bob Morrill 

of PortLana, I~E, and Vito GiacaLone of Gloucester, MA , indicate d 

that Loss of fishin9 time due to net-fouLing organisms in srring 

was minimaL, ~uch reduced from autumn. They each reported the 

presence of a green sLime high in the ~~te r column, especially i 

the inshore wdters. From their description , and from trawl net 

anll rlanktcn samples, it is concluded that this slime is the alga 

EU~~QfL~1i~. There ~ere alsJ reports of smalL jeLlyfish in 

Ipswich Bay; this was verified DY t~e presence of small 

hydrowedus~e in pLankton and trawL net samp les. ALthough nets 

occasionaLLy get clog~ed wit~ these geLatino us ~asses, fishermen 

were usuaLLy abLe to avoid them and they were not in sufficient 

quantities to reduce fishing effort. ~or rill also commented that 

many boats were in fishing areas which haa not been fished for 

four or five years. It is possible to conclude therefore that 

the populations of ~. t~[~~hi~ had not be en reduced as in areas 

ot hpavy fishin9 pressure, so the tubes in which these organisms 

live ~ere found ffiore frequently and in 9reat~r numbers than usual 

in the trawl nets. 

350 
SUMMARY Of FINDINGS 

Examination ot various samples and conversations with the Ne~ 

England port agents indicated that gelatinous organisms which 

could clo~ fishing nets were not unusually abundant in spring 

1976. In fall 1975 and ~inter 1976 the unusually heavy swarming 

of one organism, the siphonophore tiEu2mi2 £2[2' was responsible 

for the reduction of fishing in coastal waters. In spring 1976 

the occasional fouling of nets was caused by several separate 

organisms: the alga ~h2gQf~~ii~ QQ~£hglii' enveloped in a 

ge latinous mR&S during its reproductive phase, resuming a motile 

uniceLlular existence as the waters warm; the siphonophore, 

~. £g[2' found in small number~ entangled in Ehg~Qf~~li~; and 

~~ri~o!h~~ QQ[ggli~ tubes, a material often brought up in small 

numbers in trdwls. Because of increased fishing in areas where 

LittLe or no fishing had occurred in recent years, the bottom 

population of f. QQr~21i~ was greater than usually observed. As 

these areas continue to be fished, fewer and fewer tubes will 

become enmeshed in the nets. Small hydromedusae were also 

sighted. These are seasonal and their numbers should diminish as 

they comrlete their Life cycles. Each organism cited is resident 

in New EngLand waters and there is no indication at this time 

that any of these populations was abnJrmaLly abundant, nor is it 

LikeLy that there wilL be any significant adverse impact on the 

fishin~ industry as a resuLt of their presence if populations 

remain at observed L€vels. 

LITERATURE CITED 

ROGERS, C. A. 

1~7 . Impact of autumn-winter s~arming of a siphonophore 

( " Lip 0" ) 0 n f ish i n gin c 0 a s tal w ate r s 0 f ~J ewE n g l and • .! 0 

J. R. Goulet, Jr. and E. D. Haynps (editors), Ocean variability: Effects on U.S. marine fishery resources - 1975, 

p. 333-350. U.S. Dep. Commer., NOAA Tech. Rep. NMFS Circ. 

416. 

351 
CAPE 

/,) 

f 

,... \ 

,-'-

/ . 

I ': 

43 

6. HELGOLAND SITE 

Figure 21.1.-Station locations of RV Albatross IV cruise 76-02-11 at which plankton, neuston, and bottom sample were collected and examined for the presence of siphonophores. 

352 
Paper 22 

BOTTOM-WATER TEMPERATURES IN THE GULF OF MAINE AND 

ON GEORGES BANK DURING SPRING AND AUTUMN, 1976 

Clarence W. Davis 1 

Davis (1978) discussed observations of botto~-water temperatures 

in the Gulf of Maine and on Georges bank and the effects of 

temperature c~anges on fish stocks. It was generally concluded 

that the inflow of Slope Water through the Northeast Channel, 

which lies between erowns Bank and Georges Bank, was the major 

factor affecting changes in water temperature in this region of 

the Northwest Atlantic. There was a warminq trend in 1968-74 in 

both the Gulf of Maine and on Georges 8cnk, but bottom-water 

temperatures reversed that trend i~ 1175. Data in this report 

show a resumption of the warming trend in 1976 despite record 

negative air temperature anomaLies during the autumn along the 

Atlantic coast. 

DATA AND METHODS 

The temperature data have been obtained from approximately 15C 

expendRble bathythermogra~h (X8T) casts made each spring and 

autumn during bottom trawl survey cruises conducted by NMFS 

personnel aboard 81Q2!rQ~~ l~. A weighted mean or index of the 

bottom-water temperature was obtained from the area representea 

by each 2C contour interval (Figs. 22.1, 22.2) by multiplying the 

midpoint of each interval by the rercentage area within that 

interval and dividing the totaL by 100. These vaLues were 

adjusted to account for differences in seasonal timing of data 

collection between years. Both observed and adjusted temperature 

indices are presented in this report; the adjusted vaLues are 

more appropriate for comparin~ differences between years. 

INortheast Fisheries Center, NationaL Marine Fisheries 

NOAA, Narragansett, RI J28b2. 

353 

Service, 
The Gulf of M~ine and Georges Bank are analyzed in their entirety 

and by subareas of 1-deg longtitude (Table 22.1). Only those 

waters less tban 100 m on Georges Bank and mostly aeeper than 

100 m in the Gulf of Maine are considered in this report. 

RESULTS 

Both observea and adjusted bottom-water temperature indices 

reached maximum values in the Gulf of Maine in 1976 (Figs. 22.3, 

22.4>. The ad.justed autumn index of 9.3C was 2.1C warrr.e r than 

the 1963-75 mean and the adjustea sprin0 inoex of 7.2C was 1.1C 

warmer than the 196~-75 ~ean. All subarea inaices in the GuL f 

also exceeded the 1963-75 autumn and the 196b-7~ spring m~dn~ 

(Table 22.2). In the spring, subarea V had the greatest anomaLy 

(+1.1C) while subareas II and III shared maximum of 2.2C in the 

autumn. 

Adjusted mean bottom-water te~peratures on Georges 8ank in 1976 

were greater in both sprin9 and autumn than the time-series meGn~ 

for each season and reversed the sutstantial drop in temperature 

noted in 1975 (Figs. 22.5, 22.6). ALL subareas of the Bank hac 

positive anomaLies in both seasons, m)st notabLe of ~hich is the 

+2.3C on eastern Georges Bank in autumn (TabLe 22.3). This 

subarea is usuaLly 2C or more colder than the rema;nJer of the 

Bank in autumn, but in 197b wa~ o~Ly u.7C colder than central 

Georges bank and 1.0C colder tran western Georges uank. 

DISCUSSION 

Contrary to the occurrence of record cold weather conditions 

alon~ Atlantic coast during the autumn 1976 (Chamberlin and 

Armstrony, Paper 11), bottom-water temperatures reached record 

high5 in the Gulf of Maine and werE higher t~an norm al on Georges 

Bank. Because Georges Bank is relatively shallow and welL mixed 

by tide and wind, it would have been reascnaLle to expect mucr 

colder water there in autumn 1976. The deeper waters in the Gulf 

o f ~, a i new ou l d bee x p e c ted t 0 bel e s s a f f € C ted b y the col d air 

temperatures. The reasons for the positive anomalous conditions 

observed in 1976 are no doubt complex, but may be explainable by 

a time-lag in the bottom water's response to air temperature 

changes or by the fact that the large amount of Slope Water that 

entered the Gulf in the spring, indicated by the Be isotherm in 

Figure 22.1, buffered the CJld air effect, pspecialLy as warmer 

354 
Paper 22 

GuLf Water mixed with Georges Bank Water. 

The record cold air temperatures of 1976, however, may have 

.essened the current trend, onLy partiaLLy reversed in 1975, to 

ven hi£her temperatures than those observed. 

LITERATURE CITED 

~AVIS, C. ~. 

1~7b. Spring and autumn bottom-~ater temperatures in the GuLf 

of ~aine and Georges bank, 196 8-1975. In J. R. GouLet, Jr. 

and E. D. Haynes (editors), Ocean variabiLity: Effects on 

u.s. marine fishery resources - 1975, p. 241-255. u.s. Dep. 

Commer., NOAA Tech Rep. NMFS Circ. 416. 
s 

esignation and 1ocaine and on Georges 

area Lon~tude 

\I) 

I 71 -70 

n 70°_69° 

II: 69 _68° 

68°-67 

67 -66 

estern 69°_68° 

v n ral 68°-67 

stern 67 _66° 

.2.--Ad~usted mean bottom-water temperatures and 

l. s by sara in the Gulf of Maine in 1976. Anombaa on the 1968-75 mean in the spring and the 

m an in th a tumn. 

m 

pring - 1976 Autumn - 1976 

0 v anomaly °c mean °c anomaly °c 

1.0 9.0 +1.5 

ot{L9 8.8 +2.2 

+0.9 9.1 +2.2 

+0.8 9.4 +1.8 

1.1 10.2 +2.0 

1.1 9.) +2.1 

m an bottom-water temperatures 

s of Georges Bank in 1976. Anoma11 

8-7 m in the spring and the 196 

Autumn - 1976 

anomaly 

).) 1.0 

1).0 +0.7 

2.) 2.3 

12.6 +0 9 
GULF OF 

MAINE 

, 

" 

, 

- -- ---

BANK 

--- 100 M 

.' 

--- .... - . ~ .... .--- ,--

,..- - - '" I 

6 1 

- - .... -

Figure 22. L-Distribution of bottom-water temperatures in the Gulf of Maine and on Georges Bank during spring 1976; Albatro88 IV 76-02. 

357 
( 

4J 

10./ -

• 

~~ GULF 

OF 

MAINE 

---

~012 

~ 14 14S\ 

Figure 22.2.-Distribution of bottom-water temperatures in the Gulf of Maine and on Georges Bank during autumn 1976; Albatross H ' 76-09. 

358 
u 

o 

a.. 

~ 

w 

~ 

0:: 

W 

~ 3: 

I 

~ 

o 

r-

~ 

o 

CD 

Z 

<l 

W 

~ 

7 

6 

5 

I 

I 

I 

, 

h I 

I ...... ,-'.... " ,/ ,..--... -...-~- ------'''''''J ..............,' 1 .... ~ 

1 

1 

1 

//' Adjusted ...... 

" , 

1968 69 70 

Spring -

GULF OF MAINE 

71 72 73 74 75 76 

Figure 22.3.-0bserved and adjusted mean bottom-water temperatures in the Gulf of Maine during spring 1968-76. 

359 
9 

u 

0 

Q. 

~ 

W 

..... 

a: 8 

w 

~ S 

~ 

0 

..... 

..... 7 0 

m 

z 

ct 

w 

~ 

6 ~ 

~u urnf'l - .......... _ I Adjusted 

---.J -'" GULF OF MAINE 

1963 64 65 66 67 68 69 70 71 72 73 74 75 76 

Figure 22.4.-0bsenced and adjusted mean bottom-water tt'mperoture, in the (:ulf of :'t\8;ne dUring autumn I'll; -il;. 

360 
u 

0 

Q.. 

~ 6 

W 

I- Adjusted 0:: 

w 

l- I 

~ I 

I 

5 I 

I 

I 

, ~ I 

I 

0 I 

t--

to 

CD 

z 4 

« 

w 

:E SpringGEORGES BANK 

1968 69 70 71 72 73 74 75 76 

Figure 22.5.-0bserved and adjusted mean bottom-water temperatures on Georges Bank during spring 1968-76. 

361 
u 

o 

a.. 

~ 

w 

~ 

a:: 

w 

~ 

~ 

o 

~ 

tO 

CD 

Z 

« 

w 

~ 

13 

12 

11 

10 

9 

8 

1', I , I , 

I ' I \ 

I \ 

I \ 

I \ / \ 

I \ 

I \ I 

I \ I 

I \ I 

I \ I 

I \ I 

I \ I 

I 

I 

I 

, 

I 

, "' ..... ..... 

I "" I \ 

I \ 

I \ 

I \ 

I \ I 

I \ I 

,r----J v 

I 

\ I 

\ I 

\ I 

V \ I 

\ I Adjusted 

/ 

1963 64 65 66 67 

\...---.1 

Observed 

-----

68 69 70 

Autumn -

GEORGES BANK 

71 72 73 74 75 

Figure 22.S.-0bserved and adjusted mean bottom-water temperature on C.eorges Bank during autumn 196 ·76. 

362 

76