(ee aS | mil) (Fo4 Wind pw. : COMPUTER PRODUCED SYNOPTIC ANALYSES OF SURFACE CURRENTS AND THEIR APPLICATION FOR NAVIGATION by W.E. HUBERT, CDR, USN U.S. Fleet Numerical Weather Facility Monterey, California Presented at the 1964 National Marine Navigation Meeting, Institute of Navigation, December 7-8, 1964, San Francisco. The Institute of Navigation reserves the exclusive right of first publication in its official journal, NAVIGATION. December 1964 wi SS9E0O IN O TOEO g NN A ABSTRACT The available methods for estimation of wind currents, mass transport velocity by waves and permanent flow (thermohaline gradient current) are briefly summarized and a simplified computer approach is outlined. The computed synoptic surface currents are compared with monthly mean current charts and with surface wind conditions. This analysis indicates that the surface currents are greatly wind-driven. A detailed verification procedure which will use the observed changes in sea surface temperature is outlined. The use oi the synoptic current fields for computation of divergence and convergence and the resulting changes in subsurface thermal structure is described. The relative importance of the synoptic surface currents in ship routing, rescue operations and other practices is reviewed. sbewolves af sevtiorny iedto bes RRoheTsgo eyoes) , oligos aia. st nine PORE NY a j . Mit vs cue ye Pes, ran J ihslis weiulqiale e Sag tisdirommawe vita « ote. bnew ia heiebttade. si donenagal Nidinom dtiw bewgmoo o7t sine sosiue Cudemyh Detuqesn off 7 Plantes cuff, .enoitibioo balw soshiz, div bos shoe sas camel belier6b. A. nevnib-briw \ lake ms atasrvo eoslwe bial uote y nee nti Bal ned pewie) snip i - taut cl tivo Ag sali Gouingae 88 vaverent ve goes: | py i" yikeeoan oa th + aahapee inloay vatbtoty to aq iptisin ave" tei ind re shal ayoutd Ye snwomns evonlanilere 6 nuove foie any Bai iNet vtineot otab geod bed warvin wht te neg. hei 8 ate: or in Rad Marae rin | | aaa wien wl Autos ixad a ic. esiyleol isoneineg Vion bb) at8@ n9' . owed koadausit ‘eat (8901 noenidedl eg , Boa) arsaiPeny . taliston ak of ametic ae niegnosstt ROL nd aries basleas tl ‘ | | adtdo eebslwoid wo anivsitad \blobt swecutx : ee aoyeindo 3 ort | Watosete: vette, neviv ud’ {pavilewtto’ ‘ath, givelwsitieg bow) cvett espns iol bere Yi iuel we vibligen sitop phones: neue eld iw Hh | Pa. ia . ‘nn son ft Alderney oct oy nweonA O46 Bin eins rue yl entwined "i oes aontnntd \ Mabowss bi tw tis Ani Doe 8 1G bee boy TS Tait snovexebtanie unedt nent “Rob cating, yhish of qu: breve dilcow Gna ety oe baer aie) ¥ 46 siacée einemtiioggealt need wens Ole EA, teAN is 7 ; ainowa it « cabeenn encanympbee aH? ont: binibiahsih vanadate ait. ; (Ce Perino Arey Ulta UNUM eed 6 I a ill al) A St i yo a 3, COMPONENTS OF SURFACE CURRENTS Surface currents are caused and influenced simultaneously by a number of forces which vary independently from each other in space and time. If one neglects the special effects due to variation in depth, coastal configuration, runoff, etc., the current vector ata given location, time and depth below the surface (Wee) can be given as the resultant of the following components: ee =H ent Ae WE (1) where ie is the permanent flow (thermo-haline gradient current or "characteristic current" as used by Palmen (1930) and Hela (1952)), Wee is the current due to transport by wind and waves, Wy is the periodic part of the inertia current and W, is the periodic part of the tidal current. The computations which will be described here cover a period of 24 hours, and it will be assumed that semidiurnal and diurnal tidal components will equal out and can be neglected. In addition, inertial eddies will not be considered because the available quantitative infor- mation about their behavior does not warrant their inclusion in this simple technique. The two components which this study will attempt to evaluate are thus the "characteristic " or permanent transport and the transport due to wind and waves. a 2 yi yheeiciorins vinta wide fre bose whe: abate ro) aoéqe tt We pare cad Witaenneg dbin: {ioy Haletw Aaa PIS" : vl Wi Hottehey of eb vigale tnivege ati atealgey ono 8 i 9 Yotsov Insrmo odf\ (oe Honin nGveuenAGs lefeace 5H | 7 odes’ i mee) sostiwva 4d} woled diqeb fie earl? ~aottean! vestencurids “onivesiio? orf} to Hrotldsey ait 86 if oe # sl nam lie Pi pi 40 name Inetbén aittles oretitriy} wit icoinanting eae ad oi ; ek 4 (Seen) pra nae oreo aink 68 e betwee “inky He aioe avi } “oarel Ms asvew fas tw yd neqenstt of:oub wri bi a mn "a f * - a Pa “Yo rien Stig" o. eit ei v beak Nierido wht ae oy tee ¥ eerie 16 holed 6 Yeveo Piet batitroeeb od Uiw rosie clean aa i : a feihent .aturbbs vl. datcalpanq ad nis Sie wo beupe iy Binenogage "“febid Ismaulb bas Lomvotbimas soit bemuses 9d ther 2 Rae; awed MiGtil evthaiineop aldalinve sed seseodd beshiines ed ton fiw ee si , LAY st adlenlont ver? inevisw ion gecb oivbded healing LOdd | pqmedas iw youre mi noldw #enanogato2 owl ont . supine alg Sie Hoqerten MnensKertag 10°" oahiweic neds” rtd Barty oe Pewheve an i un a pbonw i015 rap o> nay any i 4 Y/ ee DE OTN M0) DUN i a a re 4, THE CHARACTERISTIC COMPONENT The characteristic component is directly related to density gradients caused by areal differences in heating-cooling and evaporation-precipitation. Although what we usually call "the permanent flow" is strongly controlled by the large-scale, more- or-less stationary wind systems, only the thermo-haline influences are included in that component here. Wind and wave effects will be lumped into one computation to be discussed later, Several workers have found (e.g. Yasui 1957) that there is a close correlation between ocean temperature distribution and dynamic depth anomalies. Neglecting salinity, one can apply the well-known meteorological thermal wind relationship in the ocean if one knows the mean temperature of the layer between the surface and some level of zero current velocity. The characteristic current is then given by: g Az bs Woo eee VE Ik (2) fr where g is gravitational acceleration, fis the Coriolis parameter, T is the mean temperature above the level of zero current, Az is the depth to zero current, and |K is the unit vertical sector. ove ; nu :¥ « Bawah . 2.3 Jie . bre onttoconantvaed ni pdenelitth isin beewed, sit" Les ilegan ow ~~ figuodttl “moran ,dlaveragusl edt dalloatne yore an Wek 2 ssonoulin ontléel-onnen) oft Yine ,eneteve baw yrenosiete ' Git woske avew bas cali? . ater inenogmee terminal beeuToh ; BS gal begayosib ed of pOkiEIyMed ano cles Ley 6 al-cned? sed? (Cee twas jo) Brwo! oved exeaow ber , bag acliudit2ib ouisraqeg? fea00 Neewiec Aquat one } - yfaqe nes ene ,yintles pabosipel .eotlemons digeb. tine OA) at qidanotteles bakw Letnei? Leolyolorootem A wea ett -asewied revel ‘edi jo MUISrE\ Mg) Hem eit tweak enc. ia Sitahatoswuts etl .yitoolev ixene> cous lo level since: at a vd nevig Aer 2! iner . {$) i ma Ty es 3 im) ae a 4 ,iwlemoisd eilolhoD sli ¢) 1 ,natiwraleods leqotstivarye: eb y¢ We 2A jinerws oqes Yo fevel Sat evods eubeidnale réem oxi) ah »@) “wolves lentiney.tiew edt al B) dae Jaen ores of et exis The determination of a representative mean temperature (T) is, of course, the critical factor in this part of the problem. The temperature structure of the ocean is certainly not constant, partic- ularly closer to the surface; therefore, semi-synoptic temperature fields should be used if possible. The only place where sufficient data is available for reliable analysis on a daily basis is at the surface so it was decided to use the FNWF Sea Surface Temperature (SST) analyses based on 84 hours of reported ship engine injection temperatures at the top of the layer. In order to include a part or the deeper tem perature structure, the SST field is presently combined with a climatological field at 200 meters depth to obtain ty ere) “22 200 (3) Finally, this field is modified empirically in areas where salinity considerations are known to be important (Cyashio, Greenland, rr Lab.rador currents). This in effect corrects the ocean temperatures for salinity much as the meteorologist corrects atmospheric temperatures for moisture content when he uses the concept of ' virtual temperature," Pei (dhatence Set iitadides et neon pelt to oisdcante ‘exude biiiersqms? oliqonys tetas Lovilenedt sontiwe ‘ty bt reeale ¢ | Jaen ter aver scaly yind.odT oldtessq We shied od thats 3 ‘ons day &P wlbed lisb 2.99 etaylode eldeils) val aldelieve a! ¢ = Tytenenetct sophie 268 TWMI ert Sen oF bedalsanks Rew 32 oa » pnety aoliasint snigne gide beatrogey to gwor $8 aa beged aonytene ( ag jo Hee 6 ebvlont c2 webto nl yj :eyal owt? 10 | got atid 16: benitimo: \ineseenq a) bi ot) Tee es an pe aiutered aad’ mietdo od diqeh eniiem 008 36 Hott lslgoerene tive be vost ote i et . “A im \Ylinilde siadw aeere ci Vile ‘nig ie, bedlibon: et biel oui wyllentt a iy . in ! orslnesse) ,doktesy.) Inetioqml ad ot nwondt os anotsarsble 4 soul sieqme? bend ant siounom tnelie nit ehiT dergonus risboe 3 oe g@linereemel cheiqeumts elsevies lciyaloimaiem at te Ae eiinilis Aa a * esutieane! loyruv’ Jo iqenndd alt eaoy st natiw insines swlaion vel, 5, THE WIND CC MPCNENT According to Ekman (1905), the direction of the wind current at the surface is 45° to the right of the wind in the Northern Hemisphere and this angle increases with depth. Recent inves- tigations reveal that the deflection is more nearly 12-20 degrees, being larger and more irregular at the lower wind speeds (possibly because of the increased importance of other components) and smaller at higher wind speeds. As the surface wind is about the same angle to the left o: the geostrophic wind, it is assumed herein that the direction of the wind current is the direction of the geostrophic wind, | Numerous empirical studies have indicated use of a single factor to relate surface current speed to wind speed. The formula of Witting (1908) appears to agree well with available data and further allows approximate incorporation of mass transport by waves in a simple expression: ae KG Hl ye (4) where Ng is the mean geostrophic wind speed for a 24-hour period. In the present work it is assumed that the current is relatively uniform and unidirectional in the turbulent mixed layer down to the thermocline (or about 200 meters). The mass transport of the waves, however, would modify this picture as it decreases exponentially with depth (Masch 1962). Therefore, if, is in meters/sec and itnowsoey es 1O nobosilh ond at 1sTi briw silt by abtioouh rt i "aevew eft le hoqenesd aanm aff , terotem GOS inode. Bs.) onal a iy AP eee OF Rn TU ee a eS Oe it PA re Yee , DIEM PORTA IAA RUM bri Soni) a 1 7 \ | ues fi a ae tee bP iy, J i i f Ve bY rie 7 ' i ; AL Dito er Vi : ay: 1 } | i f, ti ieee Mi, i ' f | f j yy { r i en ni! a iy Keg q Ae i ot Piel EA eres es nae 1 eae ae | ERG aos peas a 4 \eempeb OL-h! eles som * scoala oh tt ra iy Yidieecq) ebooga balw tewol oft 16 salient gat ae von a bane laingnegmos ieito le suneriogns bexeercnl et. (7 one “aavat 60s ,Aigels ate, ai eat uode et batw soothe odd eA ,sbeoqe bah Vian af tle ’ i aieiad baeivees ei Hy bniw aicigori nosy, eft 16 “Tal oii o. lene, — I a "a -, yo1Oe) aludle w ly dew belsoinns eyed soliuie isubiqme 4 ro alpmrot iT . beens byw ot beege lager soeiwe serttsut bas stab eldplitve thw liew sew -e of mreogge (0E 1) h it RSliow yd tqeneW Basel Io nonAoqrioce! | tiamieods Be , 2 (H) ae ye ey met, .balreq wod-ri esol bedgo belw oligotieosy Aeem ald ei 4” othe yluvitele: Ag Jcoruo orld ted) bomyeas' st tt show Mseeiy “7 4 ot of nwob yével bextm inslirhiyt editor Jenotivesthints bre m yiledasseqxe sozehiesh tl es siuipig aidt a blige « % Joy . of | i bas so2\e\etem ai ai gn moleiedt (83964 haan , Me in cm/sec, K3 is taken to be 3.3 for surface currents (ship routing and drift computations) and 2.2 for the average current down to the thermocline (convergence/divergence computations). Obviously, there is a time lag between the change of the wind and response of the sea. This lag seems to be shorter than previously believed, however, and is partially minimized by the 24-hour averaging. Since all computations are carried out in the standard FNWF grid system, u and v current components are determined at approx- imately 200 nautical mile intervals for all Northern Hemisphere ocean areas. From these components, direction and total transport (nm/day) fields are determined and stored on magnetic tape for later output in chart form or as special messages giving the currents at specified latitude/longitude intersections. 6. RESULTS Figure 1 is a hand analysis of one of the first current computations made on a synoptic schedule (18 GMT 16 November 1964). The con- tours represent total current transport in nautical miles per day; direction arrows have been plotted in the most significant current systems. One can clearly distinguish such well-known features as the Gulf Stream, Sargasso Sea, Labrador Current, Kuroshio and Cyashio. The low-latitude, westerly return flow which results primarily from the "wind component" term is well defined in both the Atlantic and Pacific. A narrow equatorial countercurrent was obtained as a result pion gl anaes aoe 0: Eo a Fe a com 00 ch true eerie) tin (ea nb bie’ + xlawoivd’ Aenokierugmos ett | vod) 9 sulvicantid ade Bins balvy att 9 wan a8 nap wot ot 6 % ‘bevelled Ylevotverq nedt setiont od 02 emoee yet eit .4 ptip eres suot+2$ off yd bestmlata yilsiting et bane jevews dulisarse | ‘aie ee mihi QWMT Luwbanta edi nl ino bones aa endelduginos Ms sone Y ‘ s PxOIGG 16 banimietes a6 einoncamos Jasimie v bile o) maleye BE mi sraiqntind fein ifs Yo! eleyiaini atim et ods! eh 5 6 ine j hoqenéy lejot bas nolineiib, etnanagmos ozedt mot”. eeoiE., / @ . etal yol ages saree io bexade Ene bertinperes vip abbeii Woo c ; iG eines of) taivic enresenmn age 26 10 mpl jstt at 3 M4 a f -atonaeseeinl abuts: pnol\ebwalted ballios EBnOweluqme? inenyo test? et Jo eas Jo aleylens bre Sap stoptt , i “noo oat ~(batl sedmavo 44 TMD Of) clubserive sitgonys 6 no sam ab yoq eolin: leviiyen mi Noganext inanyo {Ato} 28291967 ; . Inerivs InépUlagie som eid it batiolg nesd svial woe fe ot £6 aeiice) elicitation doue figtuyatteth yiseld Ase 8nd Rane ‘ ‘a -ChigsyS bas cidaows , Nreniwo. 1eberdel yee OR ehaaee 661187 i most yeaa atlves: ndohiw wotl mutes oer, banal Wa of the 200-meter temperature structure used in the characteristic component. Figures 2a and b are synoptic current charts for the Pacific and Atlantic, respectively, which have been drawn automatically on an incremental x-y curveplotter. Each chart requires approximately one minute to complete and is of sufficient quality that it can be used immediately for radio-facsimile transmission. Figure 3 is a climatological current chart for winter, It can be seen that many of the most important features are correctly depicted in this approach both in location and intensity. The problem of automatic plotting of direction arrows on these charts has not yet been solved. However, a possible substitute has been found and is now being programmed for numerical testing. Since u and v current components are available in field form at all grid points, it is believed a stream function field can be determined by a relaxation solution of the Poisson equation 9 ov au Wien = (S) ax oy This would permit plotting of a second set of lines (W ) which would everywhere parallel the direction of flow. 7, VERIFICATION A synoptic current chart would be of little value if it could not be verified and the computational scheme tuned as required, Direct 9 _ ttehetonnnila ath ak osinw snare sume i ihn ctgat te 108 ahr samen" trzomye ov aie bos “ : ; | ik , mo an. no wilottematus mead 90d overt ota vvtoenoeRsn | “Water owes enkeiperr fresh - 588 ‘rastolaaviy “x Lit | oa “Ae th duqtt vom soot te 2 bas: stetaaon co * wat ae : net abe 1 . veiw it neo Imari tecipoloteatls b e ne ut sy “:ytianatal bene, nontaoas a ge: donanast S¢et no Mwonis aokeserth te entitota OU Rennie tw aot ext ' @tuiladua eidivecg # avenge -bavloe nee ie 3 we | Rote. ti) singh hh iG ne pnobed & te enneta nl bluow Ba bree at bonut oer teaoliaunsies » current measurements in the open ocean are too few and drift calculations made from navigational fixes are frequently inaccu- rate in weak current areas, so it is difficult to make a direct evaluation. It has been necessary, therefore, to resort to indirect means which are susceptible to verification on a synoptic basis. Sea surface temperature (SST) is the only oceanographic element which permits a reasonable complete synoptic analysis ona hemi- spheric scale. Such analyses are made twice daily at FNVF Monterey (Wolff 1964), and their resolution is such that SST temper- ature changes can be determined for periods of 24, 48 hours, etc. From these changes will be subtracted the local changes computed from air/sea heat exchange equations. If the remainder correlates well with the advective change indicated by Wis aot ° VSST , the computed currents can be assumed to be reasonably correct. This method of verification is now being programmed and numerical results are not yet available, Subjective study of SST change charts and corresponding current charts does, however, indicate that the approach described here is useful. It is evident that the wind component term predominates in many areas, and that it is this term which is mainly responsible for the rapid response of sea surface temperature changes in the ocean. There are a number of modifications which must undoubtedly be made to this program; it is hoped these will be uncovered during the verification period. One obvious question is - what 10 ie eidgswonsiae yao aft at ¢ tree) enuttongson woe ‘9 tet 6 tim’ ateyinae ausgomya otelgmen nidenon cbt &, peer eg ‘ . = j ie Mite me * waa #€ bulb seiko shen ae bhi) mre ‘sive ope ae | -roamar ‘re denit AS al th eaittartcven et starts ies seats ey us | hae: aod id BS Ie aboksy net barhesatety: od ape sagan: ‘ betaqinen: ecasits leael on) borosendien we agave: eopmeda seni? | ‘gatebariod: lebaiscia artt ig ‘eeuiiaes at inne deod woe\nte A rev ols Vy et Bethea iivenk menus evttsoubs pelt soe sets joondn Videaoane ect: sal pemunas och Te elastin ” “bye Soamewory oneed steer Bh POkteotHoy. to bodien suit ag ubacie ‘oeik: ete coviaeun ISy ion ave enunovhs | vayvewutt , Beaty nits IHaTuLS paihdcgdenan se 2 eaisasia’ : inebles at 31 viaiioey Rt sued bouoaph.aendge at hat eset " | fone upeet & Yas eatertlan ban mest saber: voaeeton tet or te big avid yot ‘ilk Idkenaqees Ndindote a1 shoddy one. airl?, Bi 2 it | sNbEIC ed, ab Reyne atesoge, gosh 652 = le 2 Senogem - vibsiduim ini feasts douatey enoitmoititiom ip red e we ett effect does thermocline depth itsel: have upon the surface current speeds above the thermocline? 8. APPLICATICNS The surface current program was initiated primarily to determine divergence and convergence and the accompanying up and down movement of thermocline depth. Furthermore, the results will be used for forecasting the advective part of sea surface temperature changes. Over large parts of the oceans the currents have little direct effect on navigation. In some areas, however, they should be taken into consideration in Optimum Ship Routing. Charts of this type should also prove useful in the prediction of ice movement and in any rescue operations. It is planned to make these computations on a daily synoptic schedule (probably at 06 and 18 GMT), and they could be trans- mitted from Fleet Weather Centrals in either iacsimile or special message format if such is desired. Groups such as the Institute of Navigation may determine that there are applications in navigation which could make use of these products. ti “IaeTia® cova soe aren aeais pe sul ot rn 7 ‘ealdacumsit att man r Ya Ta ob. Tian tag tadodnint: 9¥ (bryan ameN/D wou. ult RWolt Bae qu palyneatnescs silt ais ennbbmedo: bets ‘Bore pe ‘fib atiuasy elt , Maat mined ‘thao’ ertioenmadt! lo sad Ma woyned ode tee Bee Jotau avitvebs Ort ouivenvedl hie) de: toad ohchir avai BINoTING WG Gisene il lo udneq epi « od blucda, vad? wrevewod .s4e%e. amce a Aoveniwen ng (hi lovaid®. «prison gid? @tieD ni NO Brehlencs vind cede ‘ghombrom ond. to mobibibeis Stet Liiseu oveny onle- wiatae wine obbivbo yoit bas TMD o| bee ag 16 vitor) | feinage vo alimens! sadieo ne alone ortenent to@l'l itiork i me ‘dtodisanl ordi seldove equend \posteob 2) owe yb feed) eos : nnizioiven ni Raotieoliage ow erent 3st ening st yom Howepivey, ; 7 ;@inghor Seedy jo osu wana bluco Moki REFERENCES Ekman, V.W., 1905; On the influence of the earth's rotation on ocean currents. Ark. J. Mat. Astr, och Fysik. K. Sv. Vet. Ak. Stockholm 1905-06 2 (11). Hela, I., 1952; Drift currents and permanent flow. Soc. Sci. Fennica, Comm. Phys-Math, 16(14):1-28. James, R.Vi., 1957; Application of wave forecasts to marine navigation, U.S. Navy Hydrog. Office, Spec. Publ 1, 78 pp. Knauss, J.A., 1960; Observations of irregular motion in the open ocean. Deep-Sea Res. 7(1):68-69. Laevastu, T., !962; The causes and predictions oi surface currents in sea and lake. Hawaii Inst. Geophys. Rpt. 21:55pp. Masch, F.D. 1962; Observations on vertical mixing in a closed wind wave system. Inst. of Eng. Res., Univ. of Calif. Berkeley, Ser. 138, Issue F. Palmen, E., 1930; Untersuchungen uber die Stromungen in den Finland umgebenden Meeren. Soc. Sci, Fennica, Comm. Phys-Math.5(i2). Robinson, A.R. (Ed), 1963; Wind-driven ocean circulation. Blaisdell OMS (Gag IN GCG Aude Tehove Witting, R., 1909; Zur Kenntniss des vom Viinde erzeugten Oberilachenstro- mes, Ann. Hydrogr. Marit. Met, 73:193. Volff, P.M., 1964; Cperational analyses and forecasting of ocean temper- ature structure, Rpt, Fleet Numerical Weather Facility. Yasui, M.; Cn the rapid estimation of the dynamic topography in the seas adjacent to Japan. Records of Oceanographic Works in Japan. Vol 3, No. 1. 12 Sc i .woll MoaBaneg hn dna te e200; ebay Wor fp sbobteoiven antiem 1 eteeount dw be nim csaiee EEL 4. WA ase FS ASU Bare Sasi ya reneu it yieewt 2.7 sMSRSO HAYS of) At eOlicm Telugsrl To Encltew\sedO s0S8T ) ALT +36 7 i ‘J — (eO-RO)(1) .e5 eehegged Rinegrits aoeher ie ooreliievw Bre esque Ot {S68 | val see ' ’ sUGectih pied y evrooes) feel vieWwen |, aXe bis Eset baiw beecis © kh} prikim fecthey se nnobaroed) 8010.4; MOIGar8S 4s iiete tii wind) deh oi to teal. omieye sivew Tt goaenl \ BEL oee” 1 pS \ . : Daéiniy iiss ni davhuniods ob lode nepsidouewt ly (WE { pe iE Le SMA ied ue Lis ethno d ok colt arent ‘nabaedebing MobelMa i nclieliony wneds nowindmmW loa)’ ay aA A sng c ¥f ‘ ee Lae ides morigawitoel need nvignmere Ghat V dMov seb walatienneds re gk weer (ERE TEN | JOM TPS eNe: ies iuey cana ony Wiest AGOGO 76 ‘onitan oer) bas Hea Deere hi) ; POLES | : ey re" bt Tate ou of VHS fethice! LetienwM toalh: gh POU STUER, eit . ' BESS tid hk ¥ gets cdo? Mipsetyh.od) Yer norednlie+ Gian ails Atha air. ae pbuyet at sui Sadgemoniao 19 aptoasé . . fea el Oe) Wieseibe it a i on vA ee a t, ie i a LIST OF FIGURE TITLES ENG 5. Ihe Hand analysis of computed currents for 1800 GMT 16 November 1964. Transport in nautical miles per day. Gere. Curveplotter analyses of Pacific (A) and Atlantic (B) currents for 1800 GMT 24 November 1964. Transport in nautical miles per day at 5 mile intervals. JENGi4 ele Surface currents of the oceans during northern winter. 13 Was savory te teu Pies 0) “mo indy wo ate betamn w rele: bait - {@) ottrelsA tye (AQ ottine® ko oe i ag 24 j nogenst .bs01 iedeievel AS TMS O04 SO eimetiis ie ( elevysiil deh ben 36 YOK venl mbde leokiown od i , S ' | ny ret 1einiw metho palivh sAeeod el) to elastivd aoehwe | Ne -" “ii tha] | _ OCEAN CURRENT ANALYSIS ~ooroorr-" PLOTTER y Pre ee a) ‘ ’ dz. Re: @ EN j arn an i i pe yas a) y bed L oe ~~ I (ia } : a il Fa Ari ge a! fie! i he, 1 Pare | View : < *y a ) LOT OF eae AUTOP : ee a ee 4 NOVEMBER 1964 NAUTICAL MILES ee e Nes ) (TBR ton AFD 2 iS UG ay i f ane as | ESO aS Sas] yen See iS RES ; \ Ra? or 7 : > a 4