U N CLAS SI F iE D

4f/h

ARM ED SERVICES TECHNICAL INFORMATON AGENCYARLINGTON HALL STATIONARLINGTON 12, VIRGINIA

UNCLAS SIFIED,

,NOTICE: hea govertment or other dawi gs, speei-fications or other data are used for any -urposeother than in connection with a definitely relatedgovernment procurement operation, the U. S.Government thereby incurs no responsibility, nor anyobligation whatsoever; and -the fact that the Govern-ment may have formlated, furnished, or in at way

supplied the said d ra-ings, specifications, or otherdata is not to be regarded by implication or othermwise as in any rnner licensing the holder or anyother person or corporation, or conveying any rightsor permission to manufacture, use or sell an-ypatented invention that may in any way be relatedthereto.

-NARRAGANSETT MARINE LADORA TORY

4AUATE SCHOOL OF OCEANOGRAPHY

UNIVERSITY OF RHODE ISLANDC)

Ref erence No. 63-I1

ACOUSTICS PROJECT

Seismic Refraction IVestigations in SelectedAreas of Narragansett BAy, Rhode Island

by

William B. Birch and Frank T. Dietz

jj7.Fi/-

KINGSTON, RHODE ISLAND

NO'OTS

GRADUATt- SCB)CL OF OCEANG~xT Y1NARRAGANlSEM uARIE LADoRA RJRy

Uiversity Of Rhd Isla6nd,Kingston, Rhode Island

Reproduction-Of the Material contained -in this reportin Whole or In Part IS permitted for any purpose ofthe United states overnment.

Reference ?4o. 83-1

ACOUSTICS PROJEcT

Seismic Refraction Invettigationg in Selected

Areas of Narragansett MaY, Rhode Ian

William B, Birch and Frank T4 Mietz

Technical Report No, TA

Approved for Distribution

Office of NOval ResearchContract Nourm-396(04)

wR 380"204

January , 1963

PREFACE

This paper (Technical Report Not 7A) Is a condensation of

Technical Report No. 7, N.LLo. Reerenced No. 61-5.

The seismic refraction data presenited in there two reports

Complete the third phase of an, investigation begun in 1955 for the Pur-

pose of making aVailablep sound transmission data, bottom Sediment data,

anid gaologica1 structure data for certain areas of Narragansett Day.

Sound tkansmissionm information has been reported in the following

reports:

Shalo WMte Explouive SOu-nd Trantsmdiao RuM in Q ggratnojaj by F. T. Diet, W6 B. birch, and C. V. Muiholland, N.M.L.- ReferencetNo. 61-3i 1057.

Shallow Wate E Ia Fgu lam .a iazvmaAx (Adndi by F. T. Dietz, W4 B. Bitrch, andl C. V. Mulhollaid,N.M.L. Reference No.e 58-3, 1958.

Shallowm 1"a Continuous WaM gqaM Trasiso AWj~ byF.T Dietz, W. B, Birch, And C. V. Mulhollaod, N.M.L. Reference No. 68-6,.1958.

ShalloWate ContinOus jMyj fiM Traauaglon LlMa (Adndum),F, T. Dietz, W, B. Birch, and C. V. Mulholland, N.M.L. Reference Not58-6, 1958.

Information on thel loa sediment types was given In:

AnlvZal g~f Sg1 from~e 4WS., ft", C ai, .aM _Dgg,NarraMDDStt -Bim - 1955, by C, V. Mulholland and F. T. Dietz, N.M.L.Referenc No. 56-8, 1956.

a Di1rect Measureent gj Son Velocities In a rozrans hUSediments, by F. T. Dietz, C. V. Muiholland, endW. B.BrcNMLReference No. 68-4, 1958.

The geographleal areas investigated in this report are designated

as Profiles 1 through L4. in the earlier reports mentioned above, these

same arease have been called ranges* Able, Baker, Charlie adDg. For

clarification the following list Is- given:

Present Report EI3ey9lus Rsez

Profiles 1, 2, 3, 4 correspond to Range AbleProfiles 5, 6, 7, 8 correapond to Range C-harlie9Profiles 9, 10 correspond to Rang DogProf~les 11, 12, 13, 14 correspond to Ran ge Baker

JOURNAL OFl GEOPHYSICAL RESEARCHE VOLUME 61, No. 7 JuLY 1962

Seismic Refraction Investigations in Selected Areas ofNarragansett Bay, Rhode Island'

WILLIAm B. BrmCH AND FrANK T. DiETZ

University ol Rhode Island, Kingston

, A'bstract, Seven reversed refraction, profiles have been fired in four sha'llowwater areas inNarranauett Bay, Rhode 1-sland. The results are presented in the forma of reversed travelatimegraphs and crosg-sectional representations of the strata. Seismic Velocities and layer depths areshown in tabular fom. Three ranges of velocities were obtained" (I) sediment velocities varying fron 1.54 to 1.?7 km/sec; (2) inter-aedlate velocities of 416 to 5.1 k/sec, associatedwith the Rhode 1sland forriatioin; (3) high-speed velocities ranging from 5.54 to 646 km/sec,associated with a crysta;lline third layer. in the areas under mivestigation, the thicknese of thesediment layer varies from about 14 to 52 meters, the thicker portions generally occurring inthe northernmost area. The boundary between the gediment layer and the intermediate layervaries from 23 to 45 ineters below mean low water, The intermediate layer varies in thicknessfrnm approximately 200 meters at the northem end of the bay to 58 meters toward the south,The boundary 'between the intermediate layer and the third layer ranges in depth fron 85to 340 meters below mean low water

introduction. During the summer of 1955, mation by the Pondville conglomerate, a thinseismic refraction data were obtained for four strip of arkosic rock and quartzitio eonglomer-shallow-water areas in the West Passage of Nar- ates !Quinn, 1952; Nichols, 10956], However, theragansett Bay, Rhode Island. In 1956, supple- Pondville formation does not extend into thementary seismic meawurements were made in the areas under investigzation in this paper. Thesame areas. in this paper the results are sum- sedimentary beds of the basin were intenselymarized and presented in the form of reversed deformed during the Appalachian revolution,traveltime graphs and cross-sectional represen- resulting in the formation of complicated fol&tations of the strata. whose axes trend generally north in the bay

Narragansett Bay lies in the southeastern area and northeast inta Massachusetts.part of the state of Rhode Island and is a part The locations of the seven reversed profilesof the Narragansett basin, a product of conti-- are shown in Figures 1 and 2, Three of the areasnental downwarping and subsequent deposition, are in the West Passae of the bay in the

which extends north and south in Rhode Island Quonset Point region; the fourth in Green-and northeastward into Massachusetts [$haler, wich Bay,Woodworth, and Foerste, 1899]. The bay is All references to depths in this paper are withbounded, and largely underlain, by the Rhode respect to mean low water.Island formation. a thick series of conglomerate, The 1955 data. Data were obtained fromsandstone, schist, phyllite, and meta-anthracite four reversed profiles, varing from 2.3 to 3.2[Quinn, 1952]. The Rhode Island formation is km in length. A conventional two-ship refrac-encircled by plutoni rock, chiefly granie [Quinn tion shooting technique was used. Explosiveand Oliver, 1962]. In some locations the granitic charges consisted mainly of half-pound TNT-rock is separated from the Rhode Island for- tetry! demolition blocks detonated by U. S. A.

special nonelectric blasting caps. Occasionally,Contribution 41, Naraganett Marine Lab- 21/2=pound charges of the sam e explosive were

oratoy, University of Rhode Island. This paper used. All chargs were detonated on the bottom.is baed on part of a thesis presented by William 1955 instrumentation. A single Drush AX-B. Birch to the University of Rhode Island 1 58C hydrophone equipped with a WHOI typeJune 1961 in partial fulfillment of the require- 5 .. d. phoe.eqippd .wih .a... tments for the degree of Master of Science in preamplifier was used! a a receiver The hy-Physics. drophone was connected to a WHOT two-chan-

2813

2814 BIRCH AN4D DIETZ

6 ls24' 23' 22 21,_

022 53 0 une 0- PR~ 1 0000-43 Yard

do' 0 4 P O LL 5246 -~

-15,~l2

38

0 JETTED WELLSORAVEL REFUSAL '

42

-- 1JETTED WELL03;t)o GRAVEL REFUSAL

23 62

-29 Rome PI.

1? -57Q-6 65 30

___ oain fsim6prfl-15

1,;!q MO Location of sismic profile- 156__ Z5 45 Elevation of bedrock at drilled

well or borehole0 ss Elevation of rock or boulder

'a "refusal" in borin

,6 - ri ~ Elevation of bottom of well62- which did not go t- ber

-1 -49 5 Elevation of bedrock at selected:-~points along seismic profile

All elevotionAs in feet f romn sea level mn. 1. w.25-7224- 3- '

Fig. 1. Chart of Quon~set Point arga. showing seismic profile location~s andbedrock informnatign

nel ampifier '[Dow, 19621 High- and low-pass two chamnels of a four-channell driver arnplifierelectronic filters provided water wave and [Dow, 1952j and then into a Sanborn four~chan-

groud wve nation, which was fed into nel diret wr iting recorder. A broad-band sigenal

SEISMICs 1EFRACTION21

)4 - -- 4

-6- w30

0~O

38

0

12 13-6Wairwick Pt

@ N~ ~B ~6 116 fl

'2 (678Yards

@ 0 1000 '000

Fig. 2. Chart of Greenwich Bay area showing seismic profile locationsand bedrock information.

was recorded on a third channel of the Sanborn recorded on the fourth channel. The recorderrecorder, and 1-second time tick fromn a break Was operated at its rnaxinum paper speed ofcircuit chronometer and also the rad, o-trans- 100 mm/sec.mitted shot instant from the shooting ship were The 1956 data. Methods were d igne t

700 FEET ==-- Z- ,

TRUNK FIR NG LINE NFE -SHOT CABLE SUPPORTILOA _FLOAT

- - _ -. SURFACE

SHOTT

Fig. 5. Schc-matic diagram of shot cablc.

2816 BI1RCH AND DIETZ

NORTH SO UT'

PROFILES 3 AND ZN WATE

50, 60

150 ISO M1

a v as I- LesCMOeA

ZOO' too LO.00S2

I- 003.

150 ;6 G"-'--~--- ~ A ROlCKS

400 6 0

Sis 1.50 2.45 gm.66 x6 .6 n

6AWET WATER WAVE TRAVEL TIME IN SECONDS

Fig. 4. Reversed travel-timet graph for profiles 1 A.nd 2.

give more Precise information about the sediz and a snap hook, so that the entire cable floatedment layer than were obtalined from the 195-5 about 0.3 metier beneath the water smiface. Thedata, cable arrangement is shown in figure 3.

One Vessel,- the R.V. 'Virgin z, and the skiffs The charges used were half-pound TNT4tetrylvWeie required for the 105A work. A 'shot cable' demolition blocks detonated by dui Pont no. 6was used, consisting of a 213.4-meter length of electr'ic blasting caps fired from the listeningstainless-steel cable to which snap rings were ship.attached ever~y 7.6 mieters. Taped to this cable 1046 instrumenta~tiont. A Bru.sh AX-SSC hy-was a length of two-conductor rubber-covered drophone and a two-channel WHOI amplifierelectrical cable to which a leader was spliced at were used. The broad-band output from oneevery other snap ring. In practice, an explosive channel of the amplifier was split and fed intocharge was connected to each leader in turn; two channels of a Hathaway osciliograph camnas a result shots were spaced at 15.2-meter in- era, one channel being operated at a. higher gaintervals. A metal ball float was attached to each than the other. The output from the secondsnap ring by means of a short lengt of line channel of the WO mlfe a ihps

NORTH SOUTH

0-- PRQFILES 33 D A N V 0

50 .50

DIRECT WATER WAVE TRAVEL TIME IN SECONDS

F ig. 5. Reversed trve1=ime graphis f r profiles 3 and 4.

SEISMIC REF RACTION 2817~

WEST EAST01 N&OILU Ist All WWATER O

CO55

2 31/2 Ib changs

~20

sib L2 1.00 A1 0

WOIRECnt WATER WAVE TRAVEL tiME IN SLCON66 SS~N

60 6rc

Fig. 6. Reviersod travel4ime I- aphs for profiles 5 and 6.

filtered, rectified, and fed into a third channel of the listening ship during the firing of that par-the o~cillograph Camera. A crystal-controlled ticuiar profile. T he reversed travel-time graphsoscillator provided a source of precision 100- for these profilles are shown in Figures 4, 6, 8,cps signal which was put on a fourth channel and 9. The letters N, S, E, and W foll owing theof the esciliograph for use as a timing reference. profile numbers on the graphs indicate the re-Detonation-time information was fed, into a ceiver position With respect to the shootingfifth channel of the camera. The camera was ship.operated at a. paper speed of 48 inches per sec- The 1956 data were obtained from reversedond. profiles 3, 4, 7, 8,, 13, and 14, all 213.4 meters

Results and discussion. Data were taken long. The profiles are shown in Figures 5, 7, andalong profiiles 1, 2, 5, 6, 9, 10, 11, and 12 in 10. Although the posi.tion of the listening ship

1955. In Figures 1 and 2 the circle At the end of differed in the 1955 and 1956 profi'les, it was as-each of these profiles designates the position of sumned that the sediment velocity informnation

WEST EAST00

PRFLS I N S AE

0.

00h -OW ja 0 1

3150

015

-i - 0 0 .07 1 y 0 M 15

DIRECT WATER WAVE TRAVEL TIME IN SECONDIS

Fig2 7. Reversed travel-time grarphs for profiles 7 And 8.

2818 BIRCH AND DIETZ

WEST EASTPfiOFILESWATR

~I00 [50UNCONSOIDATEDSEDIMENTS

50. IO

200 ~200250 v2a 2 lb two. 10 CONSO6LIDAT9ED' f

SEDIENTARY _

to-

3 50 4 50

3 zOK 615 - 00

0 .25 .50 .70 E00 125 L50 [15 L0-9 216 a.0 2.i5ISOO DIRECT WATER WAVE TRAVEL TIME !IN SECONDS

F g. 8. Reversed travel-tirne graphs for profiles 9 and 10.

woul brepresentative of tharaiqusi. te trdet varies fro m about 6.4 to 8.4The arows in Figures 1 and 2 point toward the meters. Exceptions are profiles 9 and 10, whichposition of the listening ship during the firing of were fired i4- the Quonset channel where thea particular profile. water depth averages 10.4 meters at riiean low

The calculations followved the method of water. The nearmsiirface sediments range fromEwing, Woollard, and Vine [1939j:; the regults gravelly sand to silt and mud [M3-uiholland andare summarized in, Table 1. In general, the Dietz, 1956].depths from the 1955 data are considered ac- Two refracting horizons were in evidence overcurate to 10 per cent; the 1956 depths are ac m ost of the profiles. Sediment velocities of 1.54curate to within 5 per cent. A 2 per cent error to 1.77 km/sec were determined. The 1 .77-kinin velocity determinations is indicated. see velocity for the Quonset channel area was

Profiles 1 through 10 were taken in the same determined from a minimUlm nubr of points.general area. The bottom is essentially flat, and The velocity of the intermediate layer varies

WEST EAST0! WATER- 0

PROFILES IIW AND 12:9

Pot- In UNCONSOLIDATED-900 SEDIMENTS 10

-- L50 4200

40 - 430041ZS [25 L

a 2 2 -chr

1.9 100

SOO .75O=DAF t 515 IO I5 0 2 5 20 000

110 A~SE MN ;- 10

ROC KS

Q ig 90 Ree6dtae-0m0rpsfrpofls1 ~ 2

SEISMIC REFRACTION 1

WES 00FILES lit AND 14W UAST

Z ' o H : oo

blIREd! WATER WAVE TRAVEL TIME IN SCONDS

Fig 10. Reversed travel~itne graphs for Profiles 18 and 14.

from 4.08 to 4.48 km/sec. There were too few liie was drawn fromn the reverse point of thepoints to establish an intermediate velocity line G2 line of, profile 10 through the pointt on thefor profile 1. H1owever, the tesuilts of a reflection 0-3 line closest to the origin. This line gave Asurvey mnade by the Gahaganl Construction minim um apparent velocity of 4.40 kin/soc, andCorporation of NSTew York in 1954 (private the zero time intercept gave a nadmum ap-comnmunaication) in the Rome -Point area indi- parent thickness to the secon d layer.cate a reflecting horizon at a depth of about High-speed velocities ranged from 5.54 to28 mieters. This depth and the reverse point 5.61 km/sec for the third layer. The high-speedfrom profile 2 were used to construct an1 appar- arrivals were well defined for the long ranges,ent intermediate velocity line of 4.48 kmn/sec. but no high-speed arrivals were seen over the

It was also necessary to use an approximate short ranges.meth od in drawing the G2 line for pro-file 9, since Measured from- me an low water, the decpthmost of the points fell along the G3 line. A to the upper refracting horizon varies from

TABLE 1. Summary of Seismic Results

Depth to Depth to Surface Layer Intermediate Third LayerUpper Ho-i n, Lower Horizon, Velocity, Layir Velocity, Velocity,

Pro-file meters meters kin/sec km/sec km/see

1 28 86 1.54 4.48 5.542 26 853 23.2 1.54 4.084 27.15 40 180 1.55 4.16 5.636 35 1307 44.5 1.56 4.168 31.19 63 130 1.77 4.28 5.6110 24 17011 32 250 1.55 5.11 6.4612 43 34013 33.5 1.55 4.3114 44.8

*All depths are with respect to mean low water.

2820 BIRCH AND DIETZ

about 23 to 63 meters. The depth to the lower Private communications (U. S. Army, Corps ofrefracting horizon ranges between 85 and 180 Enigineers, 1956; Parsons, Brinkerhoff, Hall, andmeters. MacDonald, Engineers, 1954; Gahagan Con-

Profiles it, 12, 13, and 14, in .Greenwich Bay stmetion Corporation, 1054) indicate an, appre.and running generally east axid west, lie in, ciable thickening of the sediment towards theshallow water 2.4 to 8.1 meters deep at mean east. East of Rome Point and along the line oflow water. The bottorn sediments are uniformly the Jamestown Bridge the sediment layer thick-fine, being composed of miaterials of silt size or ens toward the middle of the West Passage andsmaller, of which the first meter or so is ex- then thins out as the west shore of Conanicuttrermely soft, The sediments at the ends of is approached, A thickening of the sedimentprofiles 11 And 12 are sandy mud [Mufihaiand southward from Rome Point is also indicated.and Diets, 3956]. Sedimt thicknesses for profeil 5 to 10 are

A sediment velocity of 1.55 kin/sec was de- supported by results of a 'sparker' survey iW thetemned for this area, For the 1955 profiles Quonset chatie area (First U. S. Naval Dis13 And 14 an intermediate velocity of 4.31 kin/ trict Public Works Office, private conmunica-see was found, which agrees with the correspond- tion, 1961) and by borehole inform ation (Fink,ing velocities for the southern areas. An inter- WHOT, private eommunication, i957)mediate velocity of 5.11 km/see was computed in the Greenwich Bay area, profi,ies 11 And 12from the 1955 data, along with a high-speed indicate a thickening of the sedimnent layer fromvelocity of 6.46 km/sec. These velocities ire be- west to east This trend is further substantiatedtween 15 And 20 per cent higher than the av- by a series of boreholes Across the mouth oferage velocities for the corresponding layers in Greenwich Bay (U. S. Army, Corps of Engi-the southern areas. The accuracy of the I955 neers, private communication, 1956) as well asfigures is uncertain, however, because the sha[i by jetted wells rNizon, 1954; Pietz, Muiholland,low water made water wave arrivals difficult to and Birch, 1058].determine. Along the range between Quonset Point and

On the basis of these figufes, the depths of Rome Point, the intermediate layer shows nothe upper refracting horizon below mean low appreciable change in thickness. Between Quon-water varies from 32 meters at the west end of set Point and the northern tip of Conanicut,the profile to 43 meters at the east end. The Along profiles 5 and 6, the intermediate layerlower refracting horizon occurs at a depth of thickens from west to east, whereas dlong pro-250 meters at the west end and at 340 meters files 9 and 10 a thinning of the 'ayer occurs.at the east end. These trends point to a thickening of the in-

Conclusions. The data discussed in this paper termediate layer northward from the tip of theresulted from a sound transmission experiment, island.rather than from a detailed seismic survey; In Greenwich Bay the intermediate layer istherefore, widespread coverage of the bay was considerably thicker than in the Quonset area,not achieved. The Narragansett Bay area is and it increases in thickness in an easterly direc-structurally complex, and it is difficult to make tion.generalizations about the substructure on the The intermediate velocities are probably as-basis of a limited amount of data. There is, sociated with the Rhode Island formation andhowever, definite evidence that three layers exn agre wh velocities repored by Birch [1942],ist: an unconsolidated sediment; a consolidated Faust [191], and Hughs and Cross [1951] forintermediate layer; and a third layer, probably Pennsylvanian rocks of this type. However, nogranitie, specific velocities are available in the literature

In the area between Quonset Point and Rome for the va ious kinds of rock in the bay area.Point, along the western shore of the West Pas- A. W. Quinn (private communication, 1961)sage, the sediment layer is essentially uniform in suggests that the high velocities might be char-thickness. Between Quonset Point and the north- acteristic of a firmly indurated and metamor-er tip of Conanicut Island the sediment thickm phosed layer of the Rhode Island formation suchens from west to east. it decreases in thickness as is found near the approach to the Jamestownalong a line northward from the tip of the island. Bridge. The possibility that the high velocities

SEISMIC REFRACTION 22aire associated' with granitic rock should also be Ewing, M., G. P. Woollard, and A. C. Vine, Geo-c onsidered, sice the geologic maps [Quinn, physical investigations in the emerged and sub-1952; Quinn and Oliver, 1962] indicate a gran- mre tatcCatlPai,3 an~tByNew Jersey, Section, Bull. Geol. Soc. Am., 50,itic bedrock beneath the surrounding land areas. 2574296, 19039.

*Both types of rock niht be-expected to exhibit Faukt, L. Y., Seismic velocities as a function ofsimilar seisi1c properties, depth and geologic timne, Geophysics, 16, 102--206,

* Aeknowledgments, The work described in this' -gs .SadJ rsEatcwv eoipaper Wa upre yteOfc fN-a - ties at -high preftures, and temperatures, Geo-search under co -ntract-Nonr-396'04). We are iRt physic8 16 5774593, 1951.debted to Mr. C. V. Mulhol'land for preparationof the drawings and to the personnel of the Nar- Mu'lholland, C. V., and F. T. Dietz, Analysis of

Marin Lb ~ who din ~ coresfromn ranges _Able, Baker, Charlie, andragansett MrnLaboratory woassistedith Dog, _Narraganst Bav -1955- Ntaast afield Prograri. Appreciation is, also extended to Dr. .set- ,argaelMa

Robert Froach of Hludson Laboratories, Columbia -rine Lab. Urnv; A; I. Ref. 56-8, 1956.University, for providinig the galvanineter carnera Niohols D. Ri Bed-rock 9661o9y of the Narragana'ustdi int the 1056 phase of the work. sett Pier quadrangle, A. I., U. S. Oeol. Survey,,

We are grateful to Professors Alonzo Quinin o-tl. Quadrangle Map GQ 91, 1956.of~~~~ BrjUiesiy dCaece Mifler of the Nixnn J. D. The velocity of Sound in. sedfiments

University of Rhode Island for their helpful, con in situi Narragansett Marine Lab. Unuiv. R. L.ments. Adf, 54-12 1954.

Quin n,, A.; W.,j and W.; A. O liver, Jr., P-enhelvanianREFERENCES SySter m in the Uited States, Am; Assoc. Petrol.

Birch, F. (editor), Handbook of physical constants, Geol, 60-73, 1962.Geol. Soc. Am. Sped. Paper 86, 325 pp., 1942. Quinn, A. W., and W. A. Oliv1er, Jr., Pennsylvania

Diets, F. T., C. V; Mulholland, and W. B. Birch, rocks of, New England, Bull. Amn. Asset. Petrol.A direct measuremnent of sound velocities in Ge661i, in press, 1962.Narragansett Bay Sediments, Narragansett Ma- Shale?, N. S., J. B._ Woodworth, and A. F. Foerdte,rine Lab., Univ. R. I. Ref. 58-4, 1058. Geology of the Narragansett Basin, U. S. Geol.

DowW, An eiteriffittal poftble listening dea Survey Monograph 88, 1899.vice for detection, -measurement, and recordingof underwater found, Woods Hole Qceanog. Inst. (Manuscripot received Novemnber 24, 1961;Ref. 52-10, 19052. revised April 9, 1962.)

DISTRIBUTICN LISTNo. No.

colpiescobie's

Office of Naval Research Commanding Officer & DirectorCode Uqc. So Navy Underwater Sound Lab.Department of the Navy Fort Trumbull

Washington 25, DC. 2 New London, Connecticut 1

Director SuperintendentU S. Naval Research Laboratory U.S. Navy Postgraduate SchoolTechnical informationDivis6n Monterey, CalifbrniaWashington 25, Do C. 6 (Attn: Prof. L. E. Kinsler) 1

Director Commanding OfficerU.S.Naval Research Laboratory U.S. Navy Mine befense LaboratorySound Division Panama City, Florida iWashington 25, F. C. 1

U. S. Naval AcademyCommanding Officer Aftfapolis, MarylandOffice of Naval Research (Attw: Library)1Branch Office1030 East Green Street Minneapolie-Honeyw~ii Regulator Co.Pasadena I, California 1 433 N. 34th. Street

Seattle 3j WashingtonCommanding Officer (Attn: Dr. T.F. Hueter, mgr4,Office of Naval Researeh Seattle Development Lab.) 1Branch OfficeBox 39, Navy No. 100 Brown UniversityFPO, New York a Department of Physics

Providence 12, A. Iinstitute for Defense AnalysesCommunications Res. Division University of Californiavon Neumann Hall Marine Physical LaboratoryPrinceton, New Jersey 1 Scripps Institution of Oceanography

San Diego 52, California 1Armed Services Technicalinformation Agency Director, Columbia UniversityArlington Hall Station Hudson LaboratoriesArlington 12, Virginia 10 145 Palisades Street

Dobbs Ferry, N. ToCommanderU.S. Naval Ordnance Laboratory Woods Hole Ooeanographic Inst.Acoustics Division Woods Hole, MassachusettsWhite OakSilver Spring, Maryland 1 Bell Telephone Laboratories

Whippany, New JerseyCoanding Officer & DirectorU.S. Navy Electronics Laboratory Lament Geological ObservatorySan Diego 52, California 1 Columbia University

Torrey Cliff, Palisades, N. Yo 1Bureau of Ships (Code 531)Department of the Navy Dr. J. S. SmithsonWAhington 25, P. C. Electrical Engineering Dept.

U. S. Naval AcademyBurean of Aeronautics (AV-43) Anap s MLrlad1

Department of the NavyWashington 25, D. C. 1 Bureau of Ordnance (ReUlc)

Department of the NavyCommanding Officer Washington 25 , D. C.1Office of Naval Research495 Summer Street Bureau of Naval Weapons (RU-222)Boston 10, Massachusetts (Oceanographer) Wash., 25, D. C. I