RichardW. Sternberg Departmenr of Oceanography University of Washington Seattle, Vashington

RecenlSedimenls in BellinghamBay, Washinglon'

Bellingham Bay is a relatively large embayment located in the eastetn prt of the Puget Sound-GeorgiaSrait complex ( Figure 1). Two rivers, the Nooksack and the Samish, enter from the north and the south, respectively,and have built relatively large deltas into the bay. The city of Bellingham is located in the northeasteln corner of the area- During 19)9 and 1960 an extensivesampling program was carried out to investi: gate Bellingham Bay as a sedimentaryenvironment and to reconstructits depositional history. Sedimentshave been examined from Bellingham Bay proper, Samish Bay (Samish Bay is the southernhalf of the area and vrill be consideredas part of Belling- ham Bay), and Hale Passage,but not ChuckanurBay or Point FrancesLagoon (Figure 1). A total of 82 sediment sampleswere collected from all parts of the bay using both grab and coring (gravity and piston) devices. The sample distribution is shown in Figure 1.

Descriptionol lhe Area The easternside of Bellingham Bay is characterizedby steep hillsides rising from sea level to elevationsexceediog 1)00 ft (458 m). The beachesalong these shoresare narrovr and strevrn with large boulders- The topography of the northern and southern ends of the bay is low and flat and extends inland as- lovrlands. These lowlands (the Nooksack River Valley and the Skagit River Valley) are covered with a mantle of marine silts and clays,various types of glacial deposirs.and alluvium mostly derived from reworked glacial material (Jenkins, 1923; Easterbrook,1!62). The westetn side of Bellingham Bay is exposed. A shallow sill ( approx. 30 ft 19.15rnl) locatedbesween Eliza Island and Point Francesopens into Hale Passage,but the main enrranceto the bay lies between Eliza and Samish islands ( Figure 1 ) . The depths in this enfiance vary from 70 to 335 ft (21.4 to 102 m) near Eliza Islandl This 33)-ft (102-m) sounding is the deepestpart of a small trough adjacent to the southern and easternsides of Eliza Island, which sho'alsrapidly and connectswith the bay floor (oudined by the 90-ft [27.5-m] isobath). Except for the small depression(maximum depth 1!2 ft It8.6 ml ) north of Samish Island and the trough around Eliza Island, depths in southern Bellingham Bay do not

'Codtribution No. 365, Departmentof Oceanography,Universitv of lrashio$on, Seattle,I(/ash,

NorthwestScience, Vol. 41,No.2, 1967 6t Figute 1. Area location chart and bathymetry of Bellingham Bay.

Richard W. Sternberg exceed60 ft (18.3 rn). The area can be characterizedby a flat sheif (bounded by the 30- and 60lt 19.15-and 18.3-ml isobaths) that gradually deepensnorthward until ir reachesthe bay floor (.)90 ft l)>27.5 ml). North of the bay floor rhe deprh decteasesat a constant rate to the Nooksack River Delra, which is exposed during low tides.

PreviousWork No geological investigarionsdealing with the bottom sediments of Bellingham Bay have been made prior to this srudy. The Recent sedimentsof the Puget Sound-Georgia Stait complex were describedby $Cang in 1955, but this srudy was nor concerned specifically with Bellingham Bay. There is a report of the work done in 1959 by Roger Tollefson for the Puget Sound PLrlpar.rd Timber Company, which describesthe biology in Bellingham Bay as related rc the generalphysical conditions and circulation. Concurrent with this sedimenr study, a survey was cauied our in 1960-1961 by the Departmenr of Oceanography,University of I7ashington, to determine the circula- 'thl,s tion and physical properdes of the water in the bay (Coliias er al., f9661. investigationincludes measurements of temperature,saliniry, dissolvedoxygen, dissolved inorganic phosphate, speor sulfite liquor, and currents.

SedimentDescriDlion Laboratory analysesincluded observationof color, odor, and structure; grain-sizedisti- bution (by sieve and pipette methods); aod coarse-fractionanalysis. Besides the sutface sediment samples,select sectionsraken from the gravity cores at disrancesof ), 13, and 2I cm (1.97,5.13,ard 8.29 in) from the upper surfaceand at the botom were also analyzed, Color Only slight variations in color (wet) were observedin rhe sedimentscollected from B.-llingham Bay. In general the color of the sediments varies in relation to their size characteristics. The co.arsermaterial has an olive hue (Nar. Res. Council, Rock Color Comm., 1951), usualiy dark, while the finer sedimentshave a greenishor olive- green hue wirh varying degrees of darkness,possibly depending upon the organic content of the sediment. The upper portions ( uppr 40 cm [15.8 in] or less) of all core samplesexhibit approximately the same color relationships as the surface sediments. Below this region colors generally change to darL gray or olive gray mortled with dark gray. Often rhe dark-gray hue changesto olive gray near the bottom of the core (approxi- mately 1 m l).29 fu)). Some color changesare gradual, others are sharp. Odor Hydrogen sulfide odors were noted in sedimentsfrom ooly rwo of the surfacesampling stations. These starionswere located ilirectly adjacentto, and seawardof, the Georgia- Pacific Corporation mill and the sewer ourfall of the ciry of Bellingham. Hydrogen sulfide odor was nored at varying deprhs in all core samplesfrom the north-central part of the bay. The depth of the uppet conrac of this odor varied from aborit 5 to 80 cm (1.97 to 17.5 in) and usually continued throughout the lengrh of the cores.

Recent Sedimentsin Bellingham Bay 65 Structtne Generally, the sediment collected from this area can be considered as lacking in sruc- ture. Several of the core samples exhibit indistinct bedding because of localized coocenrrarions of shell fragments or inorganic detritus; however, lateral continuity of bedding was not observed. Textue Oq the basis of size, mosr of the sedimentsfrom Bellingham Bay can be divided into thiee major types, delta platfoim sands, bay mrids, and lag gravels. A few samples have size distriburions that are intermediate between parent types and are classified as transirional sediments. The geographicdistribution of these major sediment rypes is shown in Figure 2. Deha plalorm undl The delta platforms of rhe Nooksack and Samish rivers extend in a seaward direction from the marshes near the mourhs of these rivers to the delta fronts (at a depth of 18 fr [5.1 m]). The marginal boundariesof these plat- fotms are the beacheslining the bay into which these rivers flow. A layer of sand sras fouod to be uniformly spread over these plarfofms. In general, this sedimenr is a well-sorted medium sand, slightly skewed toward the finer sizes, consisting of approximately 85 per cenr sand, 13 per cent silt, and 2 per cent clay. The thicknessof this sand is not koown; however,a water well drilled at Marietta hit bed rock ac 24s fr { Jenkins.lc)2i . The cumuladve-frequencycurves reptesenringthe delta platform sand (Figure 3a) fall into two groupings,those strongly skewedtoward the finer sizesberween the g4th and 95rh percentilesand those thar are not. This difference,although small, allows a fwther subdivision of these sands into rype A (the straighter curves) artd rype B (those curves vrith an accumulationof fine material). AII samplesfrom type A are located on the Nooksack River Delta platform, and rhose of type B are on the Samish River Delta platform. The numerical difference of statistical paj:amerels for the two groups is given in Table 1. Ball mads. Seaward of rhe delta platforms, in the central part of the bay, a homog- eneousmud is being deposited. This mud is classifiedas a clayeysilt ( SheEard,1954) and is composedof approximarely8 per cent sand,66 per cent silr, and 26 per cent clay. Visual inspection of long pisron cores collected from each end of the bay reveals that this sedimentrype exists conrinuouslyto depthsgreater than 16 ft ( 11 m). This sediment rype can also be divided into two subrypes: rype C, those curves that ale

Table 1. Statistical Parameters oI the Three Major Sediment Types (calculated according to Inmaq 19j2)

Median Sorting Sand and diameter coefficient SiIt Clay (o) (ph;unirs) Skewness (Va) ( 7a) (Va) Delta pladorm sands Type A 2.56 0.17 0.r7 88.28 11.25 0.47 Type B 2.28 1.07 0.24 a4.09 13.34 2.57 Bay muds Type C 5.92 0.36 6.58 70.11 22.95 Type D 2.31 0.10 9.91 59.92 30.17 I-ag gravels -4.58 1.09 0.20 100.00 00.00 00.00

66 Richard lW. Sternberg Iigule 2. Lo.atioo of sedimenttypes.

Recent Sedimentsin Bellingham Bay 67 relatively straight belovz the )0th percentile; and rype D, those curves that exhibit a sharp increase in particle size between the 5th and 16th prcentiles. These types appear to be distributed sysrematically wirh rype C located in the center portion of the bay and type D found seaward of the river deltas. The significance of this disri- bution is discussedin the next sectron. Lag graoeh, A layer of well-sorted gravel covers the sill betvreen Point Frances and Eliza Island. The particle sizesrange from 3{, (0.125 mm) ro coarserthan -j+ (32 mm), with a median diameter of 4.586 Q3.9 mm) (Table 1). This sediment is composed of well,rounded, spherical, lithic fragments with abundant shell fragments in the finer sizes. It is of glacial origin, possibly an ourwashgravel (Reagan, 1906).

60

r- 20 tr_

; z

H tre5 J I lao

6 -4 2 0 2 4 5 8 tO PARTICLESIZE IN '

Figure 3. Sedjment.rpes basedon families of cumulative-frequencycurves. (a) Major types; fb) iraniition sedimenB ( represenred by dark curves.t.

68 Richard V. Sternberg Transition sedimentt, Of all the samPlesanalyzed, 12 did not fit the basic sediment classificationshown in Figure Ja. Most of these samplesappeared to be a mixture of rwo basic types afld are thereforeconsidered to be transitional in nature ( Figute 3b) ' These sedimentsare not only transitional on a textural basis but geographicallyrepre- senr a transition region that demonsttatesthe naffov/ zone of raPid change between parent types in the area. Co art e'F racti on Cam| oJ ition Sedimentarymaterial is introduced into Bellingham Bay from severalsources (Nook- sack River, SamishRiver, Ifhatcom Creek area). To interpret the relations betweeo these different constituentsand the way io which they are spread thtoughout the bay, a coarse-fractionanalysis was used. This technique differentiates sedimentsaccording to their coarse-fraction( fracdon size )62p) compositiofl and is useful in tracing the geographic origin of specific constituents (Shepard and Moore, 1954; Scruton, 1955; Shepard,1956), Thirty-nine sediment sampleswere choselras rePresentativefor the area and subjectedto this analysis. Five coostituentsaccolrnt for over 95 per ceot of the total coarsefraction of the represe[tative samples. Il/ood. In Bellingham Bay only tracesof wood fibets ale found, most wood being preservedin the form of fragments. \food fragments are concentratedsouth along the shore, adjacentto the Georgia-PacificCorporation mill (Figure 4). Their origin is not the mill itself (which would supply fibers), but the numelous log rafts located adjacent to the mill. The bark-removalarea located at the southeastside of the miil is also a soutce of wood. Directly seawatd of the pulp mill the sediment contaios numerous wood chips (approx. 5 cm [1.97 in] iong). These chips are transported to the mill in barges, vrhich are anchored and cleaned in this area. This accoun$ fol the relatively high concenffatior of wood chips found between the unloading docks of the mill and apptoximately 1% miles seaward. Within a four mile radius of the puip mill the Percentageof wood in rhe sediment decreasesto 20 per cenr of the coarsefraction (approx. 2 Per cent of the total sample). This 20 per cent vaiue is a maximum basevalue for wood concentrationthroughout the remaindet of the bay. The vertical distribution of wood in the sedimentsalso reflects the influence of the pulp mill. Near the mill the concentratiooof wood decreasesfron 70 per cent at the surface to 5 per cent at a depth of approximately 1.1 ft (1 m) wherc'as21 : miles west of the mill the depth of 5 per cent concentrationis found at 8 in (20.3 cm). Clal gall:. Many of the sedimentsamples contain varying percentagesof clay galls (Johnston, 1921). These galls are usually well-rounded,spherical aggregates as large as 0.33 io (8 mm) in diameter. A size aoalysisindicates that they are agglegates of silt-sizedpalticles with less than 2 per cent sand and 22 per cent clay They are similar in textllre to the bay muds, and are also found throughout the core samPles. The clay galls are concenffatedin the northern and southern parts of the bay (Figure 5) and account for rhe texnrtal differencesobserved in the bay muds. Type C repre- sentssamples without theseaggregates; type D containsclay galls. Although clay galls have been known to originate from severalconditions, in Bellingham Bay they seem ro form on the delta platforms afld are then transported onto tile bay floor. "In In his study of the FraserRiver Deite, Johnston (i!21) concluded, placeshard

Recent Sedimentsin Bellingham Bay 69 Figure 4. Distribution of vood fragments in surface sediments tepotted as F€rcetrtageby weight of the coa$e fraction.

Richard Sf. Sternberg Figure 5. Distribution of clay galls in surfacesedinents reported as percentageby weight of the coafse fraction.

Recent Sedimentsin Bellingham Bay Figure 6. Dis$ibution o.f terrigenous sand in surlace sediments lepolted as lrrcentage by weight ol the coa$e lfactron,

Richard W. Sternberg silt occurs in the main channel. The hard silt beds.which do nor form in rhe main channel but in the slack-waterchannels, become buried and compactedand are later exposedin the banks or occur in the bottom of the river becauseof shifring of the channel and erosion of the overlying beds. The silt, when compacted,offers consider- able resistaoceto erosion. It does not go into suspensionbut erodesslowly undir the influence of a sfforg curreor. Small massesare broken off which, by being rolled along the bottom, become subangular or rounded and form the well known 'clay- galls."' The facts that silt layers are presently being eroded on the Nooksack River Delta and that clay galls are concenrmredseaward of rhe deltas suggestrhat the disrri- bution of theseaggregates tesults from erosionaland ffaosportationprocesses ano rney should be consideredas a discrereportion of the sediment in the area. Terrigenous sand, The highest concentations of terrigenous sand ate found on the delta platforms ( Figure 6). Seawardof the delta fronts concenffarionsof sand decreaserapidly from greater than 80 per cent of the rotal sample to 10-20 per cent of the coarsefraction. There is an increaseof saod near the enffaoce to Bellingham Bay, which may reflect the stronger currents in this region. Sbell fugment:. The concentration of pelecypod shell fragments in Belliogham Bay varies from 0 ro 23 per cent of the coarsefractioo. High concenrations of shell {ragmenrs are located directly seaward of both delta fronts. The highest concentra, tioo is found adjacentto the shorelineeasr and south of the pulp mill ( Figure 7 ) . The shell materiai found seawardof the deltas is fragmental and appearsto have been transportedto its present location from the delra platforms. Oyster beds locared on the Samish River Delta platform provide a soruce for the sourhern area. The population density of oysters on the Nnoksack River Delta platform is unknown; however, they are abundant in Point FrancesLagoon (Tollefson, 1!5!). ForatniniJeratertr, Concentrationsof Foraminifera tests varied from 0 to 6 per cent of the coarsefracrion and are distributed in approxirnatelythe sameway as shell fragments ( Figure 7). Microscopic analysesof rhe tesrs were not conducted; thus futther commenr on their disuibution is imoossible.

Oiscussion Both wind waves breaking on the defta platform and the high total range in rhe bay (diurnal range is 8.6 ft 12.62 ml) are important facors ir determining the mor- phology and sediment distribution in the area. Becauseof the high ridal range, the deita platform and the river channelsare often inundated by seawater. Thus the seawardadvance of sand carried in the distributary channels is inhibited, and the sand cannoabe carried over the delta front. If rhe advancing tide is accompaniedby wiod, the resulting waves can quickly redistribute sand that has been temporarily depositedin the channels. The deitas are continually smoothed by waves, resulting io a blanket of rvell-sortedsand incised by numerous shallow (4 to 5 It [1.22 to 1.)3 m] deep) disuibutary channels. Some sand is prob- ably carried to rhe outer edge of the delta platform, but this is readily distribured. Thus the delta grows seawardby the steadyadvance of the delta front, rather than by localizedextensions of river channelsgrowing into the bay (e.g., the Mississippi River Delta). In the pasr 70 years the sediment introduced by rhe Nooksack River has had a

Recent Sedimentsin Bellingl.ramBay 73 Iigure 7. Distribution of shell fragments and Ioraminifera tests in surface sediments reported as percentage by x'eight oI the coarse fraction-

74 Richard \7. Sternberg strong inf.luencein Bellingham Bay. As much u 20 k (5.1 m) of sediment has been depositednear rhe mouth of this river, and rhe delta has been exrendedapproxi- mately 1 mile seaward (Figure 8). Ir is esrimarcdfrom sediment thicknessesthat the averagedeposition in northern Beilingham Bay over the last 70 years is about ! x 10; ytLrdss/yr(6.9 x 105 m3/yr). This rate could nor have been conrinuoussince the end of the Pleistoceneepoch becausethe growth of the delta in the past 70 yearsis nearly as gfeat as the total previously existing delta. There is evidencethat the Nooksack Rivet, since Pleistocene,has flowed into Bellingham Bay, Lummi Bay, Boundary Bay, and the FraserRiver ( Easterbrook,peisonal commuoication), which would account for frequent hiatusesin the Bellingham Bay sedimentation. Apparently the Nooksack River ofren has shifted over i1s lowlands during Recent geologic time, flowing alternately into cach of the above-mentionedareas. Therc is rlo exact way of knowing how long this river has been flowing into Bellingham Bay, or how many times it has emptied into rhe bay in the past. As shown by Figure 8, no sediment has been deposited in the southern part of Bellingharn Bay in the pasr 70 years. This signifies that sediment is being removed by marine erosion at lhe samerate that it is being depositedby the Samish River, or that the delta and offshore silts were depositcdat a time when the SamishRivet was larger (or another large river enrered this bay) and have not been strongly affected by marine erosion since rhar time. There exists an inconsistencybetween the present size of the Samish River and the extent of the sedimentdeposits atributed to it. The mean dischargeof the Nook- sackRiver is 1700 cfs (104 mr/sec) wirh a maximum of 46,000cfs (12!0 m3/sec), yet its dehaic depositsare significantly smallet than thoseof rhe SamishRiver (avetage dltschatge242 cfs [6.8 m3,/sec],maximum 5800 cfs 1163 rnn/secl). It appearsrhar che sedimentsof the SamishRiver Delta and of the sourhernparr of Bellingham Bay (as outlined by the 60-ft [18.]-ml isobath in Figure 1) are a direcr resulr of the much larger Skagit River, which musr ar one time have shifred acrossits valley floor and emptied its large sedimentload into southern Belliogham Bay. In the geologic past, the South Fork of the Nooksack River was rurned southwatd to join rhe Skagit Rivcr (Brctz, L9I)), which then formed a great delta covering 'fhe almost the entire wesren part of Skagit County (Jenkins, 1921). relationships of the South Fork of the Nooksack River, the Skagir River, and the resulting delta axe shown in Figure f. Thus rhe fearure that superficially appearsto be the Samish Delta and its offshore silt is a relict srrLrcurer€presenting the northernmost part of the ancient Skagit River Delta. At its presentdischarge mte ( averagedischarge 16,260 cfs [456 mrr,,/sec],maximum 744,000 cfs {4010 m3lsecl, U.S. Geological Survey, 19)9), the Skagit River would need to have emptied ioto Bellingham Bay for only a short time ro account for rhe size of the Samish Delta. Since the last shift of the Skagit River from the area, the only apparent effect of the SamishRiver has been to introduce fine material inro the bay. The presenceof eel grass (Zo:tera sp.) on the SamishDelta platform is import;rnr in conuolling the sediment distriburion rhere. Even rhough rhe Samish Rivet Delta is not being built at the present rime, it is srill subject to wave and curlenr acion. The eel grass protects the delta platform sands from redistributioo, thus stabilizing the sediments and rrapping the finer materials carried into the bay by the Samish

Rccent Sedimentsin Bellingham Bay 75 Figute 8. Isopach map representing thickness of sediment depocited between the yeals 1886 alrd 1956 (USC&GS Chart 6380 1st and 9th editions).

76 Richard 17. Sternberg Figure 9. Areal geologic map of westerri Vhatcod aod Skagit counties (after Jenkins, 1924),

Recent Sedimentsin Bellingham Bay River. This fine sediment accountsfor rhe relatively high percentagesof silt and clay found in the sandsthar cover this delta ( type B, Figrue 3a). Thus the Recentgeologic history of Bellingham Bay probably has been characterized by intermittent periods of deposition, first from. the Nooksack and then Irom the Skagit rivers, or simultaoeouslyfrom both. The sequenceand number of theseperiods cannot be determined with the present data.

Conclusions From rhe data presentedand the interpretationsmade, the following conclusionsmay be drawn: 1. Size analysesindicate that the sedimentsin the bay can be divided into three major sediment types: delta platform sands ( located on the delta platforms), bay muds ( covering the central part of the bay), and lag gravel (covering a shallow sill at the enffance on lhe western side of the bay). A transitional sediment type marks rhe zones of intermixing between major types. 2. Five constituents account for ovet 95 per cerr of the ccarse fraction of all sedimentsin the bay. Theseare: (a) wood fragmentsderived from log rafts adjoining the pulp n.rill, (b) shell fragments, (c) Foraminifera tests, (d) clay galls (originating on the deltas and carried ovet the delra platforms by rivers), and (e) terigenous sand transportedinto the area by the Nooksack and Samishrivers. 3. The influence of wind waves, tidal currents, and the high tidal range have a pronouncedeffect in the bay. This marine acrion is strong eoough to redistibure the sediment deposited by rivers, thus controlling the sediment disribution in the bay and the shapesof the deltas. 4. The Samish River Delta is considereddormant and in the past century has not changed. This delta was built after the Pleistoceneepoch by rhe Skagit River (com- bined with the South Fork of rhe Nooksack River) and represenrsthe nonhernmost part of the ancient Skagit River Delta. 5. At present the Nooksack River is depositing sediment in Bellingham Bay at a rate of 9 x 105 yards3/yr (6.9 x 105 m3,/yr) and in the past 7O yearshas been extended seaward approximately one mile. 6. Sedimentation in Bellingham Bay is chatactetzed as spomdic, with sediments being introduced ar differenr times by the Nooksack River, the Samish (or Skagit) River, or from both simultaneously. It is not koown how often or in what sequence each river flowed into the area.

Acknowledgments The author wishes to thank those who assistedin this investigation. Special thanks are due to personnel of the Georgia-PacificCorporation who were most helpful in providing rime and equipment for a pofiion of the sampling program. The projecr was supported by the Office of Naval Research Conract Nonr-477(37), Proiect NR 083 012.

78 Richard !(. Sternberg Literalure Cited

Bretz, I. H. 1913. claciatiotr of the Puget Sound region. Strashingror Geological Survey BulletinNo. 8, 17l-241. Collias, E. E., C. A. Batnes,C. B. Murty, and D. V. Hansen. 1966. An oceanographicsurvey li(ashingtoo, -of ^Oceanogra'- of the Bellinsham-Samish-Bay sysrem. Unil,er5ity 01 Department ph1.Spe.ral Repon \o. 12.Vo. ll. Anall.esoi dara. Mulriti;hed.t-il p. Easterbrook,D. J. . 1962,. Pleistocenegeology of the norrhern part of rhe puget Lowland, \tra'hing(oo. Ph.D. rheri<.Unireniry ol W"shingron. Mi.rori -. Inman, D. L. 1952. MeasuresIor describing the size of sediments. Joutnal of Sedimentary Penolosy, 22t 125-145. Jeflki-ns,.O. P. 1923.. Geological investigationof the coal fieids of western Whatcom County, rVashington (State) Consewationand DevelopmentDelmnment, Mines and Geology Divisioi, Bulletin No. 28, 129 p. _:-: ;-. ^L921. . Geologtcal investigation of the coal fields of Skagit County, \trashiogton. \{'ashingtofl ceological Suney Bulletin No.29, 1-60. Johnston,\7. A. 1921. Sedimentationo{ rhe FraserRiver Delta. CanadaDepanment of Mines Memoir No. 125. 31. National ResearchCouncil, Rock-Color Chart Commiftee. 1951. Rock color chart (2nd print, ing). Distlibuted by.he ceological Societyof America,New york. Reagan.A. B. _ 1006.. Someseo ogi(al siudicson norlhwe(reroVdshingron rnd adjacenrBrirjsh rerriton'. lrrnsdctronsor LheKan5r5 Academy ol SLience,20 (Patt 2t. 95-121. Scruton, P. C. 1955. Sedimentsof the easternMississippi Delta. Societyof Ecooomic paieon- tolosistsand MineralogistsStecial PubticalionNo. 3,2l-j1. Shepard, L P. 1954. Nomenclature based on sand,silt-clayratios. Joutnal of Sedimentary ' Petrology,241 151 158. _ . 1156._Marqinat sedimenrs of the Mi>issippi Det(d. Bu erin of the Ameri,an ,r.ssorrdtronol PetroLeumCeologrsA, 0: 21)--262J. -----:------, and D. G. Moote. 1954. _ Sedimentafyenvironments differentiated by coarse_ fraction analysis. Blrllerin of the Arnerican AssociaiionoI petroleum Ceologists, 38: 1792_ 1402. Tollefson. R. 1o59. puget _BioLogi(aliDvesrigation. Summary report for the Sound pulp ffrd rrmber Lompany,/l p. Unired.StatesGeological .Survq. 1959. Surfacewater supply of the United States:part 12_ fa-crrrc_siol>eba$ns rn rvalhrngron and upper Columbia River Basin. Geolosical Survev water-supply Paper 1616. U.S. Governmentprirting Office, I(ashington, D.C,402 p. puget Wang, I. H. 1955. Recenrsediments- in Sound and porrioos ot rVashington Sound- ---- and---- lake rJfashingrbnprex, \fashinsron. Universiry of Seanli, $fl.shinston. 16i t.

Acceptedfor publicaionJune 3, 1966.

Recent Sedimentsin Bellingham Bay 79