THE SPATIAL AND TEMPORAL VARIATION OF SOUND SPEED IN THE CALIFORNIA CURRENT SYSTEM OFF MONTEREY, CALIFORNIA John George Hughes DUDLEY KNOX LIBRARY NAVAL POSTGRADUATE SCHOOL MONTEREY. CALIFORNIA 93940 wr NAVAL POSTGRADUATE SCtHOOL Monterey, California THE SPATIAL AND TEMPORAL VARIATION OF SOUND SPEED IN THE CALIFORNIA CURRENT SYSTEM OFF : MONTEREY, CALIFORNIA by John George Hughes December 1975 [Thesis Advisor: J. Wickham Approved for public release; distribution unlimited. 1169788 UNCLASSIFIED SECURITY CLASSIFICATION OF THIS PAGE (When Data Entered) REPORT DOCUMENTATION PAGE . REPORT NUMBER 2. GOVT ACCESSION NO. 4. TITLE (and Subtitle) The Spatial and Temporal Variation of Sound Speed in the California Current System off Monterey, California READ INSTRUCTIONS BEFORE COMPLETING FORM 3. RECIPIENT'S CATALOG NUMBER 5. TYPE OF REPORT & PERIOD COVERED Master's Thesis; De Sr 17'S 6. PERFORMING ORG. REPORT NUMBER 7. AUTHOR(e) 6. CONTRACT OR GRANT NUMBER(a) John George Hughes 10. PROGRAM ELEMENT, PROJECT, TASK AREA & WORK UNIT NUMBERS 9. PERFORMING ORGANIZATION NAME ANDO AODRESS Naval Postgraduate School Monterey, California 93940 12. REPORT DATE December 1975 NUMBER OF PAGES 108 11. CONTROLLING OFFICE NAME AND AOORESS Naval Postgraduate School Monterey, California 93940 13. 4. MONITORING AGENCY NAME & ACGORESS(if different from Controlling Office) 15. SECURITY CLASS. (of thie report) Unclassified {Sa, DECLASS!IFICATION/ DOWNGRADING SCHEDULE 16. DISTRIBUTION STATEMENT (of thie Report) Approved for public release; distribution unlimited. 17. DISTRIBUTION STATEMENT (of the abstract entered in Block 20, if different from Report) 16. SUPPLEMENTARY NOTES 18. KEY WORDS (Continue on reveree cide if neceseary and identity by block number) Sound Speed Variability Oceanic Variability Sound Velocity Sound Speed Oceanic Fronts California Current System Mesoscale Ocean Structure 20. ABSTRACT (Continue on reveres eide if necessary and identify by block number) The horizontal sound speed in an area of complex oceano- graphic structure was described using cross sections obtained from six nonconsecutive monthly lines of STD observations at a 5.5 km sampling interval off Monterey, California. The sound speed field for each section was determined and visually analyzed. Cross-correlation functions of vertical sound speed gradients averaged over 2 m and 10 m increments M DD , Ars 73 1473 EDITION OF | Nov 68 IS OBSOLETE UNCLASSIFIED S/N 0102-014- 6601 | SSS eee (Page 1) al SECURITY CLASSIFICATION OF THIS PAGE (Phen Data Entered) a - rs == ——————————————————— ; — = a UNCLASSIFIED SeuCURITY CLASSIFICATION OF THIS PAGE(YWhen Deta Entered: (20. ABSTRACT Continued) were computed between stations. Cross-correlation coefficients between stations were computed for detrended sound speed profiles sampled at 2 m depth increments. Sound speed was an excellent descriptor of water mass features. On depth scales greater than 10 m, well defined sound speed field features showed horizontal extents of less enen 11-km in some ,cases..-On vertical scales of 2 to 10 m horizontal extents of less than 11 km were also evident. Sound speed profiles showing similarities on the scale of meee 210 m tended EO occur at 27.5 to 38.5 km intervals. °m 1473 as 1 noe he UNCLASSIFIED S/N 0102-014-6601 2 SECURITY CLASSIFICATION OF THIS PAGE(When Data Entsred) De : pains er! 0 Lf & 1 Ses repeat ,2ett 295 aode, 20eE beer) & es beaut? eieary 7 ievwade + roiloge Ieuiusey 0 e ec ae sat [i tres sans ft oy. enpda Si cake pit weds : BE Os ota 2 | ayvapo of aren = + Pete te ey The Spatial and Temporal Variation of Sound Speed in the California Current System off Monterey, California by John George Hughes Lieutenant, United States Navy B.S., University of Washington, 1970 Submitted in partial fulfillment of the requirements for the degree of MASTER OF SCIENCE IN OCEANOGRAPHY from the NAVAL POSTGRADUATE SCHOOL December 1975 DUDLEY KNOx | IBRARY NAVAL POSTGR«é DUATE § MONTEREY, CALIFORNIA 93940 ABSTRACT The horizontal sound speed in an area of complex oceano- graphic structure was described using cross sections obtained from six nonconsecutive monthly lines of STD observations at a 5.5 km sampling interval off Monterey, California. The sound speed field for each section was determined and visually analyzed. Cross-correlation functions of vertical sound speed gradients averaged over 2 m and 10 m increments were computed between stations. Cross-correlation coefficients between stations were computed for detrended sound speed profiles sampled at 2 m depth increments. Sound speed was an excellent descriptor of water mass features. On depth scales greater than 10 m, well defined sound speed field features showed horizontal extents of less than 11 km in some cases. On vertical scales of 2 to 10 m horizontal extents of less than 11 km were also evident. Sound speed profiles showing similarities on the scale of 2 [wero m tended to occur at 27.5 to 38.5 km intervals. cnigto> Yo. cea ae ab beege Pius | 2o=5 pase batisomss aoe 5 3. det? setesum e5fene dtgeh nO . sioorttoat beveta epudgest Binit Geege Se ee Ye seaki eletnow aids Yezotooh Ve Levemead ost eaee joltose dose rod Bias? Senge oande! naitelsyaes-seq19 .Bbegplens vi ° sopaus, shewbety beagp baves, cinitet: masweod PoturpoS. asaw ~ aio? Stow enolsert cessed ogi ae ‘a8 m < 36 talents ealliowy ‘arreash taadiusxe os cen. baege: < tee sazew a8 Laaeso aman wh gab sw ina [| nset sept Fea aan *ttoilele pedwole serhipag booqe at of 2. ¢5 G8 spoce 52°Rennes @ = ae EL. FET. IV. TABLE OF CONTENTS Se aN TG) Nan 8 iG yee 3 Bee BACKGROUND) —————————-———---__-_--_-_----_____--_-_ 8 1. Sound Speed -~------------------------------- 8 2. Frontal Zones ---------------------~--------- 9 3. Oceanographic Structure in the Study Area ---12 DATA COMPILATION -------~---------------------------- ee) A. DATA COLLECTION --------------------------------- 113 Be DATA REDUCTION ------—--—--—----—--—--—------__-_____ 13 USBENS ESR ses se SSS Se ea ee 18 A. SOUND SPEED FIELD ANALYSIS ---------<<2-+---=----- 18 1. Introduction -----------9-<-9------ 95 9--------- 18 2. Major Sound Speed Field Features ------------ 18 3. Comparison with Water Mass Analysis --------=- Zu Aweeopatialt and Temporal Relationships —--------- 22 5. General Comments Concerning the Analysis of Sound Speed Features ------------ 24 B. CROSS-CORRELATION FUNCTIONS AND COEFFICIENTS ---=26 Pelcceetpelon OL Method. ———————~————— = ———————— 26 2. Results of Cross-correlation Determinations -29 SOME SC eee 32 A. DISCUSSION -------------------------------------- 32 B. POSSIBLE FUTURE ANALYSIS ------------------------ 34 5 ad a aeagn dt pase enna a ee Ee Sr a a a eee igre: -c-) yigee od? St epttedé? gdigaagemses? “St . Co el A a ALTE 2 ee ee ee | CLE, on a an se - ont Dees bod Si <= Te Aes .-- - = aa eneilineaiensiil _ — + = WutT REISE araa 2 ee ee ee eee POISE AT — a J — = oe -_ 2 = 6 rm , —— — ee ‘“ “a -— nino TET Loe ae es id errs sings? tit teaadqe «6 - “;izcsecdn) adeonmO Saters= if ~j° Sayoet 26 élwylensA TSH". SOF&TALOIIOC-Sa0nD |..f - ---- fpdge to neizqissesd 7) €2’F ee eed ) TF oo. ae oy 7 Pian a oe ACKNOWLEDGMENTS The author would like to express his sincere appreciation to his thesis advisor, Associate Professor J. B. Wickham, for giving so freely of his time and knowledge during the course of this project. Appreciation is also expressed to Professor G. H. Jung for his time and assistance; to LCDR C. W. Workman and Mr. P. D. Stevens of Fleet Numerical Weather Center, Monterey, California for the use of the Calma @rqitizer; to LT Richard E. Blumberg and LT Rick E. Greer for help in reducing the data; and to Professor R. G. Paquette and Assistant Professor R. H. Bourke for their assistance in rewriting the DIGISTD computer program. Finally, special appreciation goes to my wife, Arlene, for all her encouragement and understanding during this time. avec coceke eht eeengpee ee e@lt breot iii 2388 cohwonal one said eid 4a ylest? of | 2e59 oak of nteh ta asseel -Seetoesg aids wel siese wisi 262 ssag08 .2°.% aac .% t9eee Tos ode ipomes stoglybs 4 vaj2i2es bee sels aft 20? gest .1-d 4 ol¢ To aever’ . 4 Jae bee. pete -' “it Tot siwaetlied ,Yeseseet ~sedeee Ta bas pret .& Daeteue Sad tcee2tor? of bvise pegeh off patoetes ab (iiccs% .ietpteg Teseqess OTEIGTG any eats k s cy & to \SeelzA (SE iy um af soy Rot ‘ -omlo- eit galas gosiies Pe “LNERODUCTION ae )6UPURPOSE The purpose of this thesis is to study small scale spatial variations in the sound speed field and their time changes with approximately monthly time increments in the upper 500 m of an area associated with a complex frontal region. The size and character of the variability are shown by using isotachs to contour the sound speed field over each vertical section through that region. The relationship of the sound speed field to the water mass distribution is also discussed. Cross-correlation coefficients of sound speed profiles are utilized in order to define a sound speed variability length. B. BACKGROUND 1. Sound Speed Sound speed is an increasing function of salinity, temperature and pressure. A number of equations relating sound speed to salinity (S), temperature (T) and pressure (P) have been developed. Wilson's October equation (Wilson, 1960) was used to calculate sound speeds in this study. The importance of these variables to sound speed varies greatly. According to Wilson's October equation; at 7° C, a change of 1° C in temperature results in a 3.9 m/sec change in sound speed; a change of 1 ppt salinity results ina 1.3 ‘ame yhude of ah @eiGal @ity to ssounig Sinid Seege bowen Sey ot anotiels pers =" ifs 6 me miitayV wi? ,apieet sent teeesde apésues +25) Beem toenw eas a4 Biott Beeee #2 eoiseegomi ow af Soege bawods a 2332 ¢ingecm ylodsentxorgges £ itiw tesespoces asus am’ to © ats to cetaete@s bua atia 627 Sroee wit sdetner mt eteetosl [Gt wéld@gist+o5-eibaD § .£ #)20 al bee :liog ore henge bazok” ie if inun A .#trerorg bas: s1vdEeEe was + ,(8) ¢tinilea of beogs a weed ov boyqolaweb ossad avert | 4 mrve 2tpleosinyn of besy aaw na ot éaldelzev @eet? Io-eons210QRE 124 sel if 9 pabsagoud V1 Fr \issae u4a7egmnee 42 J *I to eee - 2 to wenewtic «2 rheaqs repeeray = m/sec change in sound speed; and a 1m change in depth results in a .017 m/sec change in sound speed (Kinsler and Pry, 1962). It is apparent, in view of the normal variations in the sea of T, S, and P, that temperature is by far the most significant variable in the upper ocean layers. The error resulting from the use of Wilson's October equation was not considered significant in the qualitative evaluation of the sound speed field or in the determination of the cross-correlation function and the cross-correlation coeffi- cient, since they both are measures of relative sound speed Wartability. Sound speed has two obvious uses in oceanography. The physical oceanographer utilizes sound speed as a property to define water masses and to describe water mass boundaries, and also to infer physical conditions (e.g., vertical advec- tion) by virtue of its spatial and temporal variations. Naval oceanographers apply directly their knowledge of sound speed distribution in describing the propagation of acoustic energy in the ocean. 2. Frontal Zones A front is defined as the leading edge of a zone separating unlike water masses (Griffiths, 1965). A front is also identified in the literature as an oceanographic front, an oceanic front, an oceanic frontal zone, or a thermal front. The addition of a geographic name to any of the above indicates a specific feature at a specific location such as _ ie: ee : niyob of epeado w fs bie —heege Gores G2 nos tefackh) Seeqe based wigewde Goll RRO. & mt 2d. f ; ad slrav feeiea ada Yo weakly ei \Jenseeen Bf FO “Soe ! 35% ya ei oiedeyeqmad teed -,2 Bee 92. tT fey . Pa a wre 230 Tee aft oi oifdel-«se nasite P- e ,2dogn9 onesie to eee sie apa parsien “s eberp eft of jnsvilingee beitsb ence. a -tonievete® edt ol 26 BISER Beaqe bs | -latrnc~esote of Ban guido? 10k \_- a me - ~ pe ‘ic acangéom eto. dtodd yeds r i) be ge ¢@ ‘ it 1238 ©i eG6n wHoty 7.) aed beege = eae iva sae ‘J 1°9SR pons sop ON few Serive i bop asteen sagan S29 184 b & lb-na Isoieyity Saint Oe rogue? bes tetszewe aor to sebady S398 i (byes aamchpes aio onidueseeh ab aged a Y ~ #82900 aeno) istaest at PAL GO ei facut A nea hy 33D dt ion taiov edifnau pase vitemut i otf a3 Soilitnobs caf] ma ,3notd Siteepe ag « | hice cc 8 te mitsifihs aff “7193 io 23°. 7au3 =i? L20Gge > es the California Front, or Maltese Oceanic Frontal Zone. Fronts are characterized by marked horizontal and vertical gradients in temperature, salinity, sound speed and other properties. Fronts may be ill-defined, transient and associated with periodic vertical motions and displacements (Lafond and Lafond, 1966). Frontal zones usually occur at boundaries between current systems. They may be 200 to 400 miles wide and consist.of a number of smaller fronts. These smaller features are individually and collectively referred Ee as fronts (Lafond and Lafond, 1971). Frontal zones are especially important because the most intense horizontal variability in oceanographic param- eters is found there. As a result of their importance many frontal zones throughout the world have been the subject of intense study. Two frontal zones under investigation include the California Front (Lafond et al., 1971) between the western boundary of the California Current and waters of the North Pacific gyre approximately 500 miles off the California coast; and the Maltese Oceanic Frontal Zone (Miller, 1972) lying East of Malta in the Mediterranean Sea. In both studies isothermal contours were used to identify and describe the frontal zone. In this discussion sound speed is used as the descriptive parameter. Disregarding the question of the relative worth of one parameter over the other as a descriptor, comparisons will be made freely between this study and the two referred to above. 10 a is+sos4 sina ali a ; ts z ter jnslenew .Sentteb-Lli od yas 29hegd -t:f bes snoizo Lapis tev aiboiteg dsiw t yi Ledeen Zanox I4gnosa . (90€L eoctas band so) joan oT .ameteye s¢eerreo neewsed e6& ratione te t¢G@nunm 2 Io Jesenee Sas ebiw: :joeiion Bre viieohiviier) @26. eszuzaee2 -(I°82 Sueisi bre. bpetet) @yg07 qes.a5mts Yo veer 2< of .ssteds Bape? A ‘Sowa ai Clvow 6¢2 Secelppasds agence vapiyearni yoru ssdex l6gaes3 owt . vee ragged (fel ,.le se Banepa) sao sa _ ; MmeasztwS nzwuvettiia® sta 46 tredbaged Lim. 002 vis semkvonqys sve sklos® ‘id ( esac oteeso” geediaM ed? ban 33 i 4: Sit ot 2 <6feM Fo test oa at st foe: sae euedaoo Tanz 72 solaerrerzt alfig al .sadx” Leg 4) [a tPigecsel .tedemeteg evisels Witsoe ald -eae> pep eneT ] enw Io d2icw avis sin? ceswtert yiogs? etam od Eiiw anoak .svenis. of botastes Supporting evidence for the validity of these comparisons is derived from an analysis of the relative contributions of salinity and temperature to sound speed described by the following relation where C is sound speed, S is salinity, and T is temperature. The relative importance of temperature and salinity changes is given by comparison of the two terms within the brackets. They are evaluated from values of = and = given previously and from oe , Which can be determined from the slope of the ds temperature-salinity profiles representing this area's water masses as shown in figure 1. For the case where salinity makes the greatest contribution, indicated by the portion of the August, 1972 line below 450 meters, there results a value for = of 1.25° C/ppt. For these values the result is dee Oss G 4488)nedS:2 ; Therefore about 80% of the sound speed variability is due to temperature. Even in this extreme case, which is only locally Lt seedt lo yt 16iiar o7tielos. aif to airylote . z 1 binwe bien of stations Mem ” = | -aotekiox pith iui be r* | Be) .. #€ = 2 ~ a “7 as het Shiwet od eee = [ (ego Bis 26°. ’ 225 a _ fi Pr ‘ ' T bos .y@ietfee at 2 ,beege EBnzos* aid valetisa Bee stdgepsamad. to oontas togat evitets it aietiw ates cw eft to Asetaegnen ge o => Sas = “9 eegiaw mot? pesagisave ame! ¢* got? Realmuore® o@ asco dole , 4 i? onttoseotqey gelitesq Griatisa-t ed a a0 it 22a of seugtt-aF nwodel ae | eqt ,noltedingaes Jseeacse79 sit fom 1% eoled sui Stel az spt s* aie tot ,adgq\d *tE.2 to 702 aa mA (Sb.) « Gef) =36 of besqe Basiow sie Go 208 socda :id¢ ai aova .o2 styl ks “ie Significant, temperature is the dominant factor in deter- mining sound speed, although the contribution from salinity is not negligible. 3. Oceanographic Structure in the Study Area The subject of study here is predominantly one vertical cross section running 50 miles West from a point (Latitude 36° 40'N, Longitude 122° O'W) located just off Monterey Bay. The area is shown in figures 2 and 3. This section transects the boundary of the colder less saline California Current water flowing equatorward and the warmer more saline water flowing poleward identified as the Peoeuntercurrent", “undercurrent” or "Davidson Current", depending on the season and the author. The structure is very complex in the region of strong shear between the opposing currents due to various dynamic mixing processes. Many authors including Sverdrup, Johnson and Fleming (1942), Reid (1963), Reid, Roden and Wyllie (1958), Wooster and Reid (1963), Wyllie (1966), Wooster and Jones (1970), Milnar (1972), Brown (1974), Wickham (1975), Blumberg (1975) and Greer (1975) have treated the structure of the California Current system and related subjects. Recent work by Wickham (1975), Blumberg (1975) and Greer (1975) indicates that the current has several branches or filaments and demonstrates variability both spatially and temporally on various scales. These authors also indicate that the transverse dimension of the current features is small,.especially in the poleward flow, on the order of tens of kilometers or less across. 2 ' a aan aa l Lee BR ‘Peiaawt miss eRox> a eui~Beaeoel {°O Sér strtapeos ,M' Os ‘ac a 20ctwl9 at nepte of seta od? wie =ei 2aOfoo aft Jo ytebised ad? aoe ‘aweeteupe {itiwolt =setew JAeTaao! Fe :Tisgeeb! Haswelesz orawatd 1¢jav 2 - qoahiem)” 22 “Anserenosebayp” 4” ‘ , Ta ‘¢ pgexdh siateeyh wrotvav of¢ekie ie ii be8 ooactes quebisva eeibotomb city ban osbor ,bten) eile ) Semi Ss twmgeoc’ ~aetiy ‘seca veortswéG@ , (2° O@2) eetsos eae wiz 16 igezsza arnt —, , é jAzvov Jteow4t «|| BIcoe! due -pesae 7 adhe 2853 bac (2005) pale 1 hug atostuett? to esdonend feds La 7 yli,; toques brian yilese Sase2ut win 2¢49 Ssgectbas cals , fli mayo qa jieme al se-z:r3as? oO eyecare te §a bead 2G zabit0 ; ine » irl. DATA COMPILATION A. DATA COLLECTION A line of 16 stations, identified by 300 series numbers, was established covering a total distance of 50 nm froma reference point at Latitude 36° 40'N, Longitude 122° 00'W and extending westward. This equates to a station spacing weer nm Or 5.5 km. On one oOccaSion, August, 1973, this line of stations was supplemented by two additional lines of stations identified by 100 series and 200 series numbers. Station locations are illustrated in figures 2 and 3. The original research plan called for stations to be occupied at monthly intervals over the period from August, 1973 to August, 1974 using a Bisset-Berman continuous profiling salinity, temperature, and depth recorder (STD). Corroboration was planned to be acquired from concurrent Nansen casts. However, due to equipment problems and inclement weather, this goal could not be achieved totally. The goals were met for three vertical cross sections from August, 1973; and one each from October, 1973; November, 1973; December, 1973; January, 1974; and August, 1974. Data from these sections are the basis for this study. B. DATA REDUCTION Output: from the STD is in the- form of analog traces of temperature and salinity versus depth. The salinity traces 13 a ae! - e a > ‘1a . - a a ion | 0 45 istieh-s ,eoolJiacse at de. it. ? le solettuS fesee 8 oaixevon Bahia — ; : ; wo? ,4°OS “we sbhuvivged 27@ SRzag4 a3 a-inge ala W3evsIeY Po ‘Bins a - arn jotted .tolsesio ate ev | 6et ELE Se si0be ot Wd heoveenedgqqwe sev saokear s© Are sfense ODL = 50 lizashe ra . 7 an wt 4 Spite + @)¢aeems. Ten pbte 2 7 i? 402 toec eLeves@ai ¢idaqoe Bae i298 otk, 61¢L ,fepgee a cy ld ot i>» loge. ,ytiaiise ; \dnauetq sew 10 ’ & » OF L wrewoH stand Teog elf? ,vxitmew Jem ite if’ 303 248 ese 266 Sia bes ;cver st% tte ars 7 cE 136 °naoirsse =- “04 TIIY3GR were contaminated by erroneous fluctuations (spikes) of Salinity which had to be eliminated. These salinity spikes resulted from the inability of the conductivity cell, which is temperature dependent, to compensate properly for sharp temperature gradients. Salinity spike removal was accomplished by first comparing salinity traces taken as the instrument was lowered against traces taken as the instrument was raised. If the salinity spikes were present in both traces at the same depth in opposite directions, they were considered erroneous. The spikes were then smoothed using eye inter- polation. The error introduced by this technique was not considered significant due to the small salinity range and the small effect that salinity has on sound speed. The analog traces were digitalized for further analysis. Digitizing was done on a Calma Company Model 480 digitizer owned and operated by Fleet Numerical Weather Center, Monterey, California. The instrument converts an analog trace to a digital output expressed as inches of stylus travel from a reference point. Since stylus position is recorded every -01 inch, sampling interval becomes a function of scale. Based on the STD analog scales, .01 inch of stylus travel equates to .32 m of depth at the (0-300 m) scale and .75 m of depth at the (0-750 m) scale; a .005°C temperature incre- mene for a scale iof'5°C width; ‘and a:.002’ ppt) salinity increment for a salinity scale of 2 ppt width. The output is encoded on a seven track magnetic tape. Various codes are added as header information for identification and scaling. 14 ee - a 10. {aekiee} afolpentiap ds “5 ' ct ytinitas ean? eeererer et a ‘bert noid isidw ,ifos wives whos of3 to gitfident of? : ov ivejel4 os¢enSqgnom of ..Jasbaeqeb wot efiqe pointiae .esneibexg ust e@oas? yisetise pnlxagnoS af4 @a asadisd #eosit Jani W itod gi dueeeeqg Sabw aediqe y ssow yeds ,@rekinerib eciaogqgo ai inoie ast stew eoiiqe ad? oss aide yd Secubottal 10374 ent [lene od of sub ana>ebinpise e29 Ssttiazini®s atew sesets poleee J omisS « oo saob, saw pak eiage y2aeclee @ 202 sae i ie > @ stlcs tsf2 Jools ‘a a. seetl vd Sassieqeo . 4 Jnomtseci ett ef 7 ‘Re baerexg*s suqaue cs ‘ute soni® tated son soa gpoinns OTS aa? ae + sioqesb to m SE. of eg @ {m 08-0) edt 36 Atg iitbiw 3°2 Jo elsese 4 368 3 ije%2 “see « ao bobcods a. eoiiogn7evaAl uwspsaat ap A computer program DIGISTD, listed at the conclusion of this presentation, was utilized to read the seven track tape and convert inches of stylus travel to data values. Reconciliation of the data was accomplished at this point by the introduction of a constant correction for temperature (=208°C) and for salinity (.04 ppt) in the DIGISTD program based on a comparison of the STD data and independent concur- rent Nansen data. Output from the DIGISTD program was encoded on nine track tape, although the program allowed paper and card output as well. The output format gave temperature, salinity, sigma-t and sound speed as functions of depth at .3 m or .75 m increments listed by station and month. Subsequent data reduction was accomplished by generating an array of sound speed values as a function of depth and station number for each vertical cross section. Sound speed values were specified at whole number depth steps of 2 meters from 0 to 500 m or shallower at each station as required. Linear interpolation was utilized to assign a sound speed value at each designated depth. Interpolation was accomplished by the procedure below. Given a specified depth Dis two depth data points, D_y and Diy were selected such that the absolute value of |D-D_,| and |D-D,,| were both minimum and D Then, letting SV_ be the respective < -D < D, and SV, -l in dd: aE sound speed values of D_y and Diy , the sound speed value at depth D, represented by SV, was computed by the equation LS lo noleytynoa ett Ze oj42 Jed ioe hawt Gee | aan law esse od Tqwes asigte lo matted nica eitt te Sede igieqos saw sonb-ed? 20 Tush cages 292 ASTI 29SEOD sna sency ato wos: meroyad GPRIDTA aid wl Laqq $0.) ysinilse 102 Saeee Dn ‘a ges « ude Gee 609 20 mielxeqney AY Tish) of2 eats soqruo paab: lis wetebes set Apmenfole «eues dost? oni 10 > +00) Smgtue sa? 0 fed as. zegiue biso flit ac hee 4P bacce Baa 2~aayce oyeiniise * i. (eta wi betazil efcaemeorni @w 2. to m €,- 38o i ret vo teweriqgneios aay ocldoches e2ab 2heuE an vaviev beoega Srv0e 36 bali “40 esot= teuiteer dose 1202 tec ef) ; f2 deush 2eGmn Slot #2 belttioagqs Stas te sowed fete sem O08 - Ne ie _ § “betes of becllion saw nolissloqpaga™ gat ¢biqel Sedenoltash does ai biicaaz © mavih woled siubés0%@ iosisa aise . 9 Dr - oC ,eraiog 2a 1 = \~ oan il} 40 sulev yrs (% tra p_ VG. einbsesl etatDG £49 >a i Si ,» pl Dates i= i= Ve vi 6o } to sbelaey Sosqed + begun 26% weastqes ,@ A measure of the error in the interpolated value of SV was determined by calculating the mean absolute difference in the sound speeds at the two data points, D_, and D,, , averaged over one vertical cross section. N ) ISv,, - SV MEAN SV ERROR < A = N l al Since the maximum mean absolute difference was .036 m/sec, the resulting error was considered insignificant. Holidays in the data were also filled using the same linear interpolation technique. Instead of specifying one depth, D, N depths dD were specified such that and where ov is the sound speed value computed at depth D,- In all cases, holidays were only localized and of limited extent. 16 steucrltth opofeads assem wif? paiselyols> yt back ‘] fm . -athted €265 ced adv 26 abseqst -ocitaes soc Isgtexsy ean isyo a ut we - \ veh | ‘@ 2 Aoaas va mame, 7 rs -_ fet ~— = - a : * As ¥ ( tomer atites eieloeds «ssa cumticent) 6m icaottiaptee! Gegsbianes asw toss9. paeboeim ia onten belts? eela stow stab of9 na ayebt, fipsege ic Seusaak infios? aclrelogunease ‘+ Asue Bellieses s204 A nitgeh 4 ae t>.G.~.» @} : {+ i- i? t « ia - I Pe | e / = 7A - —“ ‘ i ft. iiry Aeecta@ Potroe soit 2: 7 esew eysihiiont ,2a0@ When interpolated values of SV had been assigned to all depths at 2 m increments, mean SV gradients were calculated for 2m and 10 m intervals. The statistics of these gradients are found in the section on analysis. « vitsattess SAT elevaedmk «OL. ahs ends = 7 7 jlece no o6htnwe @42 @) Baws] OF x a ay = IIIT. ANALYSIS A. SOUND SPEED FIELD ANALYSIS i Lntroduction The sound speed fields are illustrated in figures 4 through 11. It has been stated previously that sound speed is used by physical oceanographers to identify water masses because, as a function of salinity, temperature, and pressure, it reflects changes in these variables. Higher sound speed tends to imply higher values of both temperature and salinity and vice versa. Since temperature is the dominant factor in determining sound speed, higher values of sound speed may reflect merely higher values of temperatures with lower or equal values of salinity, and conversely. The two basic water masses in the area are "southern" water and "northern" water and their identifying character- istics are higher salinity and temperature and lower salinity and temperature respectively. Sound speed features such as sound speed maximums and minimums reflect the presence of least mixed portions of the respective water masses. In considering sound speed as a water mass descriptor, sound speed variability due to pressure was ignored due to shallow depths, less than 500 meters, of the region analyzed. 2. Major Sound Speed Field Features As stated previously, sound speed field features will now be discussed in terms of the features defined by Lafond 18 of) 4 6 ey | &' =: =e 1211p Jtl = 1p & w hi rh! al tiv c jsidqmet Ajod lo aseier xodplit yvilamk atjepl {i atm abieit Beoge bayée SAF 'setounes .weidatitey cassis al aspnedo agce 460 asuisy sf0med to supley tofolt yvlezeme sticods bee tedaw el 1 weteaw 6 6 boega Sovose pain =o} gf to enhte? of Bbaeaeusatibd od we yiewoivety bacads aaed esd 31 “ELS mh: of etedgqsap0nssco [scieynq yd & ,“2isilee Io aeizosnut «2 BS pl tat Gee yoinlise sodpid sti 2iupietn bas emimixem base to ,~s7etem 00¢€ nat? peal «i ee —— Jo2 ,Viemoivety Getess 2A 7 mt eee Fs notsoubpssak - @ eiagess sonif .s2esev safigia .beege Devos oe “raedj7z0n" Sa v Vieviaseqdesi sinvteiee tet self Io encijszoq beck saaxy oF aubh viilideizeag bisst Sees? bavo2 z0¢aM = aad ouarond, (0966) ,211967) .(1967)>¢and (1971).°°oIn their discussions Lafond and Lafond defined characteristic features of the thermal field including ridges, maximums, minimums and frontal zones. Similar features were found and identified in the sound speed fields of this study. The following discus- sion considers the individual sound speed field features and their significance. A ridge structure is indicative of a minimum in the horizontal sound speed distribution and represents a colder less saline water mass. Examples of ridge features are shown at station 108 in figure 4 and station 316 in figure 9. The scales vary considerably between the two examples. Lafond and Lafond (1966) defined ridge features with horizontal Seales on the order of 15 nm by 45 m to 50 m in the vertical. Sound speed maximums and minimums are defined by closed isotachs and indicate extremes both horizontally and vertically. Maximums represent warmer more saline water masses of limited horizontal and vertical extent. Well defined sound speed maximums are illustrated at station 316 of figure 7 and station 316 of figure 8. Less well defined examples are illustrated at stations 305, 314 and 316 of figure 10 and station 304 of figure 11. Similarly, sound speed minimums represent colder less saline water masses of limited extent. Sound speed minimums in this study are not as well defined as are maximums and ridge features. An example of a sound speed minimum occurs at station 108 in figure 8. rg +69 o233 i tedsetes naan ene ortus tne - eephhe enituiand biel? san? oF Sei ti oat eitisnhoeb: Siumty ows iff avewied yi daessbianoS sfiok of .\yhate aids ‘ie ableit beaqe't reovaqe: bie solasdiaterh Beece Basoe viva! gspbia 25 agla@nsxad .3aam ‘3s snvet sxew @seggeet sal ipgia 2am : test hesgea Engicoe fechivibeal e7 ateb .eoneoh2 im hs & 30 ovidestBat 21 esadovuzse sobis ~iemaxo bec) .é@ennde 260408 neowted ’ a wi COS bee O48 eenieage agented bortetta0lil a ete to + stupkh ad Ge Boe ELE enolsase bre 25? eanésete aeguted bas’ 48 4 «o¢h Sdod te onfA .Gf emppil- ai 50608 “ort wtienS teseegaqg esn0s -lasaoke racije® eoetT .(i1 wageit). BICE 5 moo sto to Jivens ml! ozs. sens vistas tenga ,weveruh .estoenela as Acuwias pais i?os i2et jleess 5 £ > $0 saa te elves eue i 3 > F208200325 & sd _ 4 is gel it? cut? teabiva B2-9% Sol 3eri anen na 63am iy 5 2 ) “ a & ~ f z : 5 3 - Posi as -\SOR . SUS ¢ #34 o> ea o&als Sizes ft lj i i: ‘anm Jesae >1 & Oe: ¢ i7eek « by “ 4 i 5 éf ~ 3 j sage 15 @2eJa012 A : »ibheto teage aAngor et at BY wilew Buseor 21? month. It appears to approach the surface in August fe2oures 4, 5, 6, and 11). During the months of October (figure 7), November (figure 8), and December (figure 9), the feature migrates progressively downward. During December (figure 9), its intensity is greatly diminished and it is virtually absent during January (figure 10). This feature is seen world wide. An extensive body of research exists indicating that it is the result of a combination of heat flow across the sea surface and wind induced mixing in the surface layers. 3. Comparison with Water Mass Analysis To further analyze the use of sound speed as a water mass descriptor, comparisons were made between the results of fares Study and the work of Lt. R. E. Blumberg (1975). Blumberg, using the same data, delineated water masses by analysis of temperature distribution relative to sigma-t surfaces. In his analysis Blumberg defined northern water as low temperature, low salinity water and southern water as high temperature, high salinity water. The cores of these water masses equate to sound speed minimums and maximums respectively. Comparisons of sound speed field features and Blumberg's analysis yielded close correspondence in a majority of cases, as illustrated in the following examples. The northern water centered around station 108 and the southern water at station 111 in figure 12 correlate well with the ridge feature centered at station 108 and the dip in isotachs eM 2S toss roupad ok @iy Iau 26 atten . 12.1% o7ugt}) teckeokdh Sep ite acu . sawnweb vierladeyer se es apd wa Beth lated yhacomy af (2 samen wat ite sweet) Ywtuasy onda saundele enti wd stores »eorhSns a4 agayioas tag) seic% a@siv aoe) Pu '? =t sd? a2e7lace Bede wis se ‘ iSFRR) ve sytecnoJa® p4 .sebiw Bose 7 oShyps atuos te anoelzecnm- wast ‘tl 2 bosentayvl li aa (je (Jae bovow Beestnep ootsew adaee rare ‘hit te s 20 Siyort acts oi 4-760 Saiv Ses -s9e@)awe sea st = 8 T6¥, ~ — 212m soc e2telzcqune agg hg 5 A SF 1s Pec os base VE ‘OS ,4265 atez orf? pales reweidrieste2b Stir eisqis7 To" attesy ia eievisas Siqal ne crt wai: wae 2 (rimiigsgea fpid oreifs hoes? fuuee OF ervageg ‘tiew 7 Setivly witvisas a's in. si winort me LEI mpiztata “3a “Ot! te Sm beagegews anise ote at station lll in figure 4. The northern water at station 314 in figure 15 and station 310 in figure 16 show excellent agreement with the ridge feature at station 314 in figure 7 and 310 in figure 8. The southern water at station 315 in figure 17 is in agreement with the dipping isotachs at station 315 in figure 9. The southern water at station 305 and the northern water at station 303 in figure 18 are in excellent agreement with the sound speed maximum and dipping isotachs at station 305 and the ridge feature at station 303 shown in figure 10. One point of interest that was demonstrated by a comparison of the two studies was the ambiguity in the origins of some sound speed field features. Some are derived from horizontal water mass variability and others arise from vertical motion. An illustration of this is found at stations 306-305 of figure 9 which indicate a sound speed maximum and minimum respectively. Comparison with station 306-305 of figure 17 indicates the feature is the result of vertical motion in the water column and not due to the water mass structure. Vertical motion in figure 17 is indicated by the displacement of the isopycnals and isotherms in step with each other. 4. Spatial and Temporal Relationships Inspection of the sound speed field revealed systematic relationships among various identifiable features. Comparison of the three lines of stations for August, 1973 (figure 4, 5, and 6) did not show the continuity of any uniquely identifiable me a ea sf) wosdate Se tad a ‘ielieaxs 6ede di i |, Speed: wa: OT ‘Oc 3826 38 S20 36e1 sd - | i [ Tw ltt 56 tatew sretoom ggT .6 « +a) 3 etvaséet eigges ult fo iw inomacrys “a ail > "y «a = aofieed i” 29007 noni foe sctT ,? molt nts £ F ite 3 2Bii Ff £66 gossesea ta iIsisw «4 16 Sar ‘uetteew Deege Eewoa ade ddiw saaee | OE ceigsse 36 pandae) eebhe ers Bde 202 poltedawe Je Sell 2852 Peoseta: Io salogh © BJ =e sine suis W 2915024 cows add Yo; } wie ; m1 ™ 226 eto aSirzeal Cisit beege bm Ts SiSt Sterso Bie Yrtlidsixnsy caec -adae i » 2G nocssztagil[i aA at Ceiaw & egynit 24 2 . j e =<) ,¥levi Gest mens . ‘ di aS2G5I bat Ts . i Omploo tatew of) al F Ti t 26708 Lf 59 t2 y Sti 20 2 wane? Ses fn; : 3 9 Digos wds eO7 ; 5 ' PuQihisv oftums esidane Lal Gacigsae Fo .aeaif sorts “19 ware ton Sib) water mass feature through the three sections. This indicated either that the feature's spatial extent was less than the spacing between sections, 10 nm, or that it transited the area at some oblique angle. This last possibility is reinforced by the flow patterns shown by Wickham (1975) and Greer (1975), who described the region's currents using drogue measurements and geostrophy, respectively. On other vertical cross sections certain similar features appear on succeeding sections. A comparison of the 300 series sections for August, 1973 and August, 1974 (figure 6 and 11), indicated the presence of similar sound speed maximums, indicating a warm more saline water mass, at 400 to 450 meters depth in both sections. The positions of the features differed by 33 km between the two succeeding August sections. The feature in the August, 1974 section also appeared more well developed than its counterpart of the previous year. A comparison of October (figure 7), and November (figure 8), indicated the presence of similar well developed sound speed maximums representing a higher tempera- ture more saline water mass at station 316 in both sections. The feature in the November section appeared to have decreased definition and a greater depth by approximately 100 m than that in the October section. Similar ridge features indicating low temperature lower salinity water also appear in both October and November sections. Their positions vary, wath. one located at station 314 in.the October section and ee ae ae ‘ie os a) a Seed botexnibal » tary . eae ZtSe", ee, os a an 22 gery esyl aw Joes Indinge, a sawed *. wi? boyioneats 44 onde 29 jan ot » eaalsoa& s ei yo Itdieaoc tee] eiff .efpns. supdide se (4°00) matvocd wi awode enesbaeq wolt ont vd : - pla tivo "adios: et bedivoeoh ore tet —_ - ‘Ieqeast )Yequstecsey Ona so anaes Is) eaoidose amore leolJser-2zedte@ siz.gmeo & ,apelones enlbseesous a6 a6 Si. .daweguad sol ancitoes i S sdes@enty ort) BetsolGai .(L0 bee sc Lise ston ocraw @ eniteotSai . em iJod os mtqed eteten O2a J Ai Sagie@ed mi Ef ut Bees ib sees ein eis fi 7Sen? sit. anol vor rx sc! -sootiewvel Lilow sroq Bes itiowot) 43 4cc50nm5s A .téesyY eto SoG Sisasiinat-~, (F srupid) 4@S%3407 s me Isa¢ ites bad 2s 7 5 i ae? - 9 {+ ¥, 40979457 — a .™ eo a | oe 7 La: -B0°2327986 tescota0 usdd/ ee atu tereqmeas vol pal “nave tw iusde3o0 nis ul ST geezese Ze bessunl_ ease @nd the other feature lcoated 22 km east of that position in the November section. The November feature also appears more well developed than its October counterpart. Frontal zones present in both October and November sections also are Similar. The frontal zones in the November section are greatly reduced in intensity from the October frontal zones. The position of similar frontal zones also varied between sections by 11 km, being centered at station 311 in October and station 309 in November. A general comparison of October, November, December, January, the 300 series section for eeeuce, 1973, and August, 1974 (figures 7, 8, 9, 10, 6, and 11) demonstrates the difficulty of predicting short-term changes. No obvious similarity of features exists between the vertical cross sections for the months of August and October; November and December; and December and January. The pair of vertical cross sections for October and November and for August, 1973 and August, 1974 are the only sections showing obvious similarity of structure. 5. General Comments Concerning the Analysis of Sound Speed Features In concluding the discussion of the analysis of the sound speed fields, it is appropriate to make a few general comments pertaining to the overall analysis. First, visual scanning indicates that sound speed fields define the "Character" of the water mass more sharply than does the temperature or salinity alone. "Character" refers to the Shape, definition of the core and extent of the water mass. 24 “2ee lelewOR add St-aeeds Ieto072. emt — fovv0 oe govt ~iiemetnt ni begs , cel» aenta Laseccl taliniia 36 aor acisase Ja berzsgneo paind wad if of) “oe Lapraeg A aedarvow ot Of ne a owtves 0G wit ,yrewast ,rodmepet ,8:.. s@abpid) stez submid Gres even F oteto i besg Io yilwolitlb off eetacee swwi2tse? So «iéerliehs syoivdd tc etttwe els sof saciscee ganze s ioehe: hat ,;tedesoed Ene sodmevell £ +37 29% eevltooe seoto lacigzey 36 si) Ste *TU) ,fawpud Dee tT Qs stufoeute to viirgeliatia. 4 cr centaeonago giinemnod Lag [$2206 See tls heer oF ——- ‘j 1m opbaseoe2®> ers vaelielones Ju2agosaen af @) ,ahtok® 2 sic fleteue anf? of gnindasieg Ot ‘as ijmmoan 20.79 Ssveriint 142 ston sehr aetew wit to “z f‘omcedd”" .Ssegi6 yetnilas ad 2203 Sam dts: 29 Ore ates eff Se welothitvel-% _ Water mass elements which are small in spatial extent and have a definite shape and a well defined core region are meeustrated sat station 316 in figure 7 and at station 305 in figure 10. Water mass structures which are large in extent, have less well defined cores or cores below 500 meters, and lack definite shape are illustrated at station 310 in feoure 8, Station’ 316 in “figure 9, and station 315 in figure 10. The extent of mixing is also evidenced by vari- ations in the character of the water mass structure, variations in the slopes of the isotachs, and the overall complexity of the sound speed field. The loss of the 1487 m/sec isotach in the core region at station 316 from October to November (figure 7 and 8), a reduction in the core definition, an overall lessening of isotach slopes, and a reduction in the complexity of the sound speed field over the two months illustrate this. Several comments pertaining to the problems of acoustic propagation are also appropriate. Since the sound speed field ioameme controlling factor in the propagation of acoustic energy, its complex structure is significant. Sound speed minimums tend to channel acoustic energy decreasing trans- mission loss locally. Several poorly defined sound speed Minimums are illustrated at station 110 and at station 108 in figure 4, and throughout the vertical dimension of the ridge feature at station 310 in figure 8. Lafond and Lafond (1971) found much more pronounced minimums, in terms of temperature, in their analysis of the California front. 25 Sound speed maximums, on the other hand, cause local divergence of acoustic energy. Well defined examples of sound speed maximums are illustrated at station 316 in figure 7 and station 305 in figure 10. It is apparent that the sound speed field in this region is very complex and attempts to describe it would require numerous samples of the vertical sound speed profile at suitable intervals in time and space. aa CROSS—-CORRELATION FUNCTIONS AND COEFFICIENTS i. Description of Method Cross-correlation functions and cross-correlation coefficients were computed to provide a more objective measure of the small scale sound speed field variability, including characteristic "correlation lengths". Two different methods of analysis were employed, one involving sound speed, the other its gradient. One method utilized the sound speed gradient averaged over 2 m or 10 m intervals to derive a cross-correlation manction (Rxy). As defined in Bendat and Piersol (1971), where N is the total number of depth data points; n refers to a specific depth data point; and x and y are sound speed gradients at depth n and station X and Y, respectively. The two Stations are separated by some horizontal distance from 26 = : —_ ' -, ave on + gi TE ; a og wah 4 ; =e. a“ bo asiqmexn Ssalted Liew ypiege obezec a © , b> ti 05 sei tede da hetastavill sen. sapnines | a > ae jot tfotegie =f 22 -.OL Sega? al @6¢ -nolisaze baat _ => Wiew ei aoipez elite ni- bf612 bacqe Sa ~~ "U7 Ee etingst Sivow 411 edi«oes] O68 be ' it @, desires 36 @.i}o7qd Saeqd Savoe *so8qe 7 VIWSIIIGIAND GHA SHOT TOMIT wOTTAsaIa09-98 . , ° ‘ >: Aizu io isats a | bofzes co solsyitosed sitalortec-ésore lings >i wt ooltzaloexrteo-ee6 > a - - at) 3 7 A ce) wecy as=éV DIGt? Seagqe Gaywow selese i i=a¥I0O0" . Fj ° De Lame so | ; ue SDs be u od Pptillsyu pods: ‘Ae - ¥ 7 i - fovea FF Tr on r2q9o 4m ese a) anol seg mero 16 Station intervals. Space lag in depth (n) is zero in all cases. The use of the sound speed gradient Pte De ae aaa) S khd 4g07rdnds where g; is sound speed gradient, and Ve and Va41 are sound speeds at depths Zs and Zend respectively, had the same effect as using a high pass filter. Smaller scale variations in the sound speed profile were emphasized and larger scale variations were de-emphasized. Rxy provides a numerical value repre- senting the small scale similarity in shape between the sound speed profiles at stations X and Y. The other method treated detrended sound speed values at 2 m depth increments to determine a cross-correlation coefficient RHOxy. As defined by Bendat and Piersol (1971) N (==) (y--¥) RHO my el: ae 2 a a ON N N ee —, 2 he (xe-Rhsls sleltyszy) = n=l where N is the total number of depth data points; nis a specific depth data point; x and y are detrended sound speed values at depth n and stations X and Y respectively, separated by some horizontal distance from 0 to 16 station intervals; and x and y are the means of the detrended sound speed values at station X and Y respectively. Detrending was accomplished using the relation 27 irtys ss 15<] vie . = ¥ St ' = { A an + ae ee 2 ~ 1 ~ ee VY ime .teolberp buege Sanve Ze 735s >» ~od Tema ae Loess 71 & BHO é oye! a & i be eo = § 7 a > \ MIO: a t +1 -(aafz5 gasq dpid’ atgae saew siltozq be Torq yak i yiite. Gbls eissa itéais sf Bo 3 hea * ettoeb. 7 . bes i es rigmes wucliseia ta anit a ‘sam isit?o set 4 “a io eSnteanesoal Ade ed re ly -yxOka 4 aé in Isszo7 ef’ ak -Saiog #740 Tqet % Jove Ons oon iqah ge ingath Issoo0s lz0d snpey ay ors ¥ brew mensey ¥Y ban Z aos solizalo=: edt v(n,X) = V(n,X) - yea_ .) Vy (n) where v(n,X) is the detrended sound speed value at a specified depth n and station X; V(n,X) is the sound speed value at depth n and station X; and the last term is the mean value V computed at a given depth n from the sound speed values Vv; at each station i=l to NSTA inclusive. Detrending also produced the effect of a high pass filter. Again detrending emphasized small scale variations and de-emphasized large scale variations. In this example comparing the results from using the sound speed gradient and the results from ising the detrended sound speed values would be equivalent to comparing the output of two high pass filters with the latter having alower cutoff frequency. Both methods emphasize small scale variations but, between the two methods, detrending emphasizes larger scale variations. RHOxy gives a numerical value between -1 and +l representing the small scale similarity between the shapes of the sound speed profiles at station X and Y. Normalization allows meaningful comparisons between RHOxy values determined different stations and months. Results are displayed utilizing two different methods. In one method, Rxy and RHOxy are plotted as a function of distance between station X and station Y. A reference station (Y) is designated and identified along the Y axis of each graph. RHOxy and Rxy are then plotted at the correlated 28 = yA, : . iv eo a eae: neh Y ai; {a's Te a sas off al oma? Joel et Bon tk noiszase bauoe stt ei (KR. a) sh soisadge Bae [2 3/13 a2asaq doit.a Ta 2natie 18 212 .48i3e8 eflese teozel , o59q. Davee behterseab odd et OR -— xi2 aoyt i teqeb aevlip 6 ta ie wWietiva: ATU of int sore i 3; Lifeliae wiave ifema mos aiqewke tits at sanoigas ieilore heege tenoe eff: - suclev ieoge baa bebsasaaaig yvie@ 40d enoltalasv i*sieeraws L¢ Gas [= “sews nse ed? Io sogats mig availa noltsxilamios= °) Goniatsotsal aault : niqei® esa ativueshl ¢ “1 hate yaad «bods { qoatese neewsod i* Jpait Boe badgaenpiesd “th Gah wae ROMA, J oa a station on the X axis. Each figure contains eight graphs, one on top of the other. Scales, with values ranging from = to... 03 sect, are not indicated on the graphs .001 sec” of Rxy since their purpose is to show relative values of the cross-correlation function between adjacent stations. Values of RHOxy vary from -1 to +l as indicated. Graphs of Rxy and RHOxy are shown as figures 19 through 22 and figures 23 through 28 respectively. Another method is also used to display the cross- correlation coefficients, RHOxy. Ann xn matrix of the cross-correlation coefficients, RHOxy, is established with each RHOxy being computed from a specified station X and station Y as indicated. Contours of equal cross-correlation coefficient are constructed and the resulting fields appear in figures 29 through 31. A maximum value of unity appears along the diagonal of the resulting field, with symmetry about the diagonal. 2. Results of Cross-Correlation Determinations The cross-correlation functions derived from the sound speed gradients averaged over 2 meter depth increments for the month of October, 1973 were computed. The results are shown in figures 19 and 20. These cross-correlation functions were characterized by small correlation even between adjacent stations. The cross-correlation function was also computed from sound speed gradients averaged over 10 meter depth increments for October, 1973. The results are shown as dqe.w ddgaa le Se = re “Te? poatpgeet ao le? chiw xaleo’, -vaedee ahd ‘got: wiscwy wile #O tind gt 2h ose one 8. ea" = io ¢t#lev ovideley wode oF #1 Stegugg od E inapatbs sseweed nod tren? ao ks. i iS it _fetooaivat we f+ o@ I- mow3 vase 4 7.7? bes 15 nd ee ET ao Seif eye “ “eon > dae oiaitibes tala Beviras 2 ys Be oi (fe lioegeey etna 2ee of tothe LOE ee Sreeed teh Seseixe notgal Ke mot at weer OL av iuosrevs ors tae row sumeteth egigaseee Sepaet of4 souls besciegita Leni‘trey 'feem of sah utttidaleav od? To dour 2m = ~ viuab etasiolPMess aplsefetis>-asers SFE i ot bedgeqane Soke ssurlav beeqe -bovoa ft eL- Std Ban, evel Yemenst Ever * scrTe 8S @opwads €) se2vel? a6 1 visoeguee 1 m ,O£ ,V ewerpti ine ag ait ot strggok vasuted colseli { - i” moi:Yslepe>-egocs eff af aholsar iti] om dew sestesat a "a 2eiitsv esnatoilisos norisalerice ai outa avisesor DS ores tps aT 86. asel Go me 2 al .200] ; tjeecpttiecs notselerios yisnerper® ae” To e.s2r6o edt? Ilstovo : “o-eaet> Sid asaso Jae vi 19 godaseiS 6 nifgiv asel Fog oo tecilgiad Yo aeiget edt .sonse misgsse ies C08 fnoitvare naewisd (88 Das 82 .ff 4 Correlation length, as defined here, is the distance between successive maximums of the cross-correlation coefficient. This parameter specifies the distance between stations having similar characteristics on the vertical scale of two meters or so. Correlation lengths were on the order of five to seven station intervals, 27.5 km to 38.5 km, euerng August, 1974. Correlation lengths for January, 1974 were quite variable ranging from a distance of 5 stations, meoekm EO 10 stations, 55 km. 31 —— > Joatetelh off Gs , 62a Gee a ’ - Lor cotjelorey-aaase, Sie Bey ' reeQtad oct océetele emt As a a iQ a a > a r" ~_ 7 sv at? so euételsopanade deftate yi : i . —< - nf ie ih A> Oo sise aol sotte[s3365 tt 39 aisten OW. we 7 a7 es Sf of ood ©. 0°94, eiaoeetad epiteda caves od vi2© .Vieucst 20! appre doljelese® .6TOF «Jet next osiones sidsizay | #3 tl 22 .omokseve OF ¢ to sorav236 « i - IV. CONCLUSIONS A. DISCUSSION This discussion has addressed the problems of horizontal scund speed variability. This was accomplished through subjective analysis of the sound speed field and through computation of cross-correlation functions and cross- correlation coefficients of sound speed gradients and detrended sound speed values respectively, for stations along a vertical cross section. The results, indicating a complex picture of sound speed variability as a function of both time and space, are of interest and concern to physical oceanographers and specifically to naval oceanographers. Physical oceanographers, it has been shown, can use sound speed as a descriptor of water masses. Its use enhances differences between water masses as compared to the use of Salinity or temperature alone where changes in salinity and temperature between water masses are of the same sign. For this reason sound speed permits high resolution in defining the structure of water masses. The naval oceanographer is interested in sound speed as an oceanographic variable which is the controlling factor in the propagation of acoustic energy. The complex sound speed fields in this study area result in equally complex fields of locally varying acoustic intensity. The nature of the effect of the sound speed field on the propagation of acoustic "i lotr’ lesonme sow als? hl tdatsed B As _ ur z i : : a to Bmsidew, ae beguethhs asc 70 LeguoRil i ist) heege Sarge ef? 20 ateylens 2 5 Fe bn ene tageus® sokgnlettos~-ea01D 20 NOLTE ci cy iSeee beoage Saved to etietni?teoa mise yo. \¢Levlessqast asulsy. beeqe Gavel be >a ozfw2a% ofT ,qni¢os@ @a075 ak miso © es #2 iLidsbaay Saece Onavoa te4 oi useseat hap taeystnl Jo ese .S9eRere ine avec Gt yileqitjioage bas ered veat! sad +1 ,enesqeagoaseno Is . 2 Hote Gefew bo), to%glipEesd> fs ef agian 24 Seon 2awW msewsed alts ta ecole segderedned tO “in £60666 ada Aamdind sivism rag Lesus bioe nos - : — t4Jew 20: etytIerF . é *-c0%nb O41 togigasponmssdo fsvan 7 ib dsliw detisy Siigeipece 2iTewoSea Io mottspsqo ‘7 wy i ‘i t.tews esde yBuse Bids at sd oi ' taetet witepvese pitytay yilese cig of ef pfsh? Seite Lovee 282 Fo -. + energy depends on the frequency of the acoustic energy. For frequencies such that the wavelength is much less than the scale of the sound speed field feature, refraction occurs in a predictable manner which is not dependent on frequency. For frequencies whose wavelengths are on the order of the Size of the sound speed field feature or larger, scattering eccurs as a function of frequency. This would mean, for sound speed field features on the scale of two meters, that scattering becomes important near the frequency and, for sound speed field features on the scale of 10 meters, at the frequency where f is the frequency, C is sound speed and L is wavelength. It is apparent that the influence of complex sound speed fields, like those treated in this thesis, on acoustic propagation should be studied. A first step in such a study would be an objective description of the environment. This thesis provides such a description. First, for vertical scales of variability greater than 10 meters, it was demon- strated by visual analysis of the sound speed field that the horizontal extent of such features was, in some cases, less 33 mn a. vo vane 3 ee, ate 7 A? wom. peasy ‘elt _ = 4 We o a in et Lay oo Ai toatja> (odes enue ewer oa i oo Juneau som we deter Senasai oldesal 40 vat ote so owe adspactovaw snotty sae i to eyytee? GLelt besge Barros sAy: ~w ola? oYEmeperS to noltona 's” ' to efeane et no aseeges7? Blatt | rT uit seu Joatioguk esdocad git ‘ off no Bo1ud6eet? Sfeitd Bbeega hasoe a7 sc « BOB OG2i . 2 ‘Tt a cl D ,epesrpes? oft ed 1 ay ; ii aig ted? teesaggs- ek .! @) baetveaoss oendy etil-s Ev i:tese od Slgodst roles | 50 esiigaeaeeh ovsetoetdo aa ad . zi ritaees & disgie anb ivoig $ 2 wewme ye ilidaizay 20 a 2 uiere i je aieglian® lawaivy yd 7 2m Fas} iave te aontxe isd - > than 11 km. Second, for scales of vertical variability between 2 and 10 meters, it was demonstrated by the weak correlation between adjacent stations that the horizontal extent of these features was again less than 11 km when the variability was integrated over the entire sound speed profile. The correlation length provided a measure of how often sound speed profiles similar on the variability scale of 2 to 10 meters repeated themselves. Correlation lengths on the order of three to five station intervals (16.5 km to 27.5 km) were predominant. B. POSSIBLE FUTURE ANALYSIS The application of other analysis techniques to the present data is suggested. One such technique is to lag the cross-correlation coefficient in the depth direction to investigate the effect of internal wave activity. Another is Calculation of the cross-correlation coefficients over smaller segments of the sound speed profile, as opposed to correlation over the entire depth range, to localize the centers of variability or homogeneity. A third variation would be to compute the cross-correlation coefficients over several different vertical sampling intervals of depth, in addition to the 2 and 10 meter intervals used here, to study the cross-correlation coefficient as a function of the variability scale. Future research projects might include extension of the present area of study to include stations further east and west; occupying stations at time intervals of a few days or a week to describe short term temporal variations; and sampling ae Shorter horizontal intervals. | idoisey Seoiee Roemaiias J ise od yd Gages Lew - aT | ony “shied ono. 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Oe aa & SUOTILIS UdeMJOg WIG :eTeoS AaVeM UIBYANOS :::: sTeudAdoS Tuo mmu Adem UIIYIAONS A SUTDYyIOST — -“° STATION CORRELATION OF SOUND SPEED GRSOTENT FOR GGT 1973 ogee Rxy 311 312 Rxy Rxy Rxy REFERENCE STATION 314 313 315 y 1 === cae) 3 17 3 14 3 iL STATION 3 08 306 $ 02 Preure “19. Rxy by station. (Gradionts averaged over 2 m intervals) 53 STATIGN CORRELATION OF SOUND SPEED CROGTENT Pi Geir ors 302 REFERENCE STATION - 306 305 Rxy Rxy 307 5 a eee | : i as aa! 31? 3 14 3.11 STATION 398 3 05 3 02 Figure 20, Rxy by station. (Gradients averazed over 2 m intervals) 54 OPS. OSs. © eae CORSELAT I eee we ero 312 REFERENCE STATION 5 eple) ION SF SOUNDS SPEED SRAGTENT Figure 21. ixy by station. is >> 2 a = See a aE (a, (| 3 i7 3 14 3411 STATION 3 08 3 05 3 02 (Gradients averaged over 10 m intervals) 55 % [oe eyes ¢ wir? He ° . etrmerbasd), x ont : ut -'* — CORQE moe OC 1973 302 REFERENCE STATION 30S 307 “ ““"“"""" | i ie (Rice eaicals | inn naa | nara ss) 5\7/ 3 14 311 STATION 3 08 3 05 3 02 Figure 22, Rxy by station. (Gradients averaged over 10 m intervals) 56 Bre On OCORRECATLON OF. rSQUND “SPEED FOR GCT 1973 REFERENCE STATION RHOxy peas Neal < 3 iL. STATION, ,S 08 3 05 3 02 17 3 34 23. K.1Oxy by station. iy] ‘ a= ip ) ih [ere I — = erent < STATICN CORRELATION OF SOUND SPEFO FOR Sor "i373 REFERENCE STATION 305 taal 3 17 4 Figure 24, RHOxy by station. 58 STATICN CORRELATION OF SOUND SPEED FOR JAN 197¢ BECBRENSE STATION RHOxy We be: RHOxy 315° - RHOxy ea ai Vee ae Pe Meal | 316 RHOxy 342 3 44 311 STRTION 3 08 3 05 3 02 Figure 25. RHOxy by station. 59 < i a / ~ — = - ee . i ™ ~ —— _ hal | ¢ > = = - » a ; ie hee a -_ ie ~~ ————— — F — i Pd el J — yl 7 é ws, 4 = a \. a oe —_—— ay gm ~~ — oJ we yore Ue STATICN CORSELATION OF SOUND SPEFD FOR wal 1974 ' RHOxy 30Z ga 0 ci Wy Le a i, RAB: na 2 oe | a ae RHOxy .¢) 303 RHOxy 4 30 RHOxy REFERENCE STATION ' 305 = (al Figure 26, RHOxy by station. 60 STATION CORRELATION OF SOUNG SPEFD FOR AUG Is REFERENCE STATION Sf 3 14 Figure 27. RiOxy by station. 3 4i STATION 308 H i ers wee : \hbsete qd yO AS. . . STATION CORSELATION OF SOUND SPEEG FOR AUS 1974 RHOxy REE STATION RHOxy es RHOxy 0 = 307. RHOxy eRe) 308 RHOxy 0) Do | i See I On| es) 0 ae ep aS Sake 3 14 311 STATION 3 08 3 05 3 02 Figure 28, RiOxy by station. 62 el het AO (4 99" ~ ‘. = . =. ae ene S miter ww iboede | ; NOTLYLS STATION CORRELATION OF SOUND SPEED FOR OCT 1973 STE SO € SOE e 20 ) 3 = ation coefficient (RxXOxy). Figure 29, Contours of equal cross correlation Note the area of high correlation vetween station 307 and 303, 63 NOTLELS Tre We eve 80 € SOE STATION CORRELATION OF SOUND IBeEBOFOR. JAN 197 Lo ° | > bade STAT LON Figure 30, Contours of equal cross-correlation coefficient (RiOxy). ee UN CORRELATION OF SOUND Seen FUR suo 1o74 wen mo 000 a0 ate = ae | . | | 0.5 0.4 Tw! ” Peat ae NOT LHS soe TLE wre SO € & 20 STATION Figure 31. Contours of equal cross-correlation coefficient (RHOxy) > = 6 = Pas —- a bt Oo a ASS=«) uw uJ uw - (a) win ) Be (v4) Ph Qa fen Yo Ses | me ~- Oo > Z =) oO aS) a =) uw. ~aoOere Ww a > Ivza <4 _ ty) a! a (=) Ww =) AW INE rx mm <_t mw a oO Ww N FRWM es) =) yo SZ Y Qwest 2) He CC —e WwW NHN ryan) lu e a _ WreO~DO J — ato Oe 3 Sf) + 7a) Ne eae (je xe Soa LoS a " Pee HOIST LE Awe Fae Yo kX Nat WwW uu ke COA e woe a. 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