3 1

W90029D

DRAFT PUMPING TEST TECHNICAL MEMORANDUM

SUPPLEMENTAL MOM Rl

GROVELAND WELLS SITE GROVELAND MASSACHUSmS

NUS ARCS I

WorkAuignmentNumber04-1L32 Contract Number 68-WB-G1 17

August 1990

3 l

W90029D

DRUl PUMPING TST TCIIIIICAL MBIIORANDUM

SUPPLMDTAL - RI

GJ10VUAi1D IIULS SIT GROVaAJID MASSACIIUSTTS

- Corporation

IPA llork Aaaiv-nt No 04-lLll Contraot llo dl-tll-0117

Autuot 1990

rAIILB OP CQftDI8

Draft PullpiiiCJ raat ractmical -ralldbull Suppl-ntal - RIPS

Groveland Wellbull Site GrovelaDd llaecbuaetta

10 I~IOII bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull bullbullbull 1

zo - 30 -DQ Hft llftDICX(JGy bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull

40 -DQ Hft ampVAUIATIOII bullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull bullbullbullbull 41 Data Ra4uction bullbullbullbullbull bullbull bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull 4 2 Data Evaluation bullbullbullbullbullbullbullbullbullbull bullbull bullbull bull bullbullbullbullbullbullbullbull

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ID IWIHCUCOPCAPIUU- bullbullbullbullbullbullbullbullbullbullbullbullbullbullbull I

AIPDDII A - CALCIILAriOIII AIPDDII I - -Ill IOIL IMPLIS lllll

GRAil IIIZ AIALYIIB

10

Draft ~ing Teat Technical _randua Suppl-atal - RlPBGroveland Welle Site

Groveland Maaaachuaetta

I~IOII

Thil technical MatorandWD au-rhea the perforunce of EPA Work Alli9naent No 04-1L32 EPA Contract Nuaber 68-W8-0ll7 and evaluation of the puapin9 teat recently performed at the Groveland Wella Superfund Site alon9 with the related prelibullinary capture zone analyaia and dhcuaaiona and recoMndationa r~ardin9 upcoain9 data evaluation activitiea The teat waa conductecl aa part of the ManaC)-nt of Mi9ration I) RIPS that ia currently underway The raw data collected durin9 the tnt ia not included in thia aubllittal but will be included in the upcoain9 RI Report aubaittal rhe calculationbull perforeed for the analyaea are provided in Appendiz A

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r~fo~middot~~~f~~~~ bullt~0~t~ ~middot~~~9 t~idtfebullh~=~~tt ~te~tfehr~t~tcs drift aquif and to providbull a databaabull fr which to projbullct botb the current capture aone of the Station llo 1 wll aftd the capture aone of the well in the paat when it vaa puaped at a hiCJber rate tban the current rate Tile data waa alao to be uaed to recreate flow conditione in the paat when both the Station No 1 aDd Station llo 2 vella were in operation The 9oal of the capture aone analyaia ia to deterwine whether paat contination detectod in the ltatioa Ro 1 Hll could be relatod to thbull troundwater continant plUM centerecl around the Jlill PondJohnaon CrHk area fte followint eectiona deecribe the perfotunce of the _int teat data reduction and evaluation activitiea and tbe reaulta of the teet evaluation

lO _IS ftft -oGr

The Station No 1 well waa puaped continually for a period of 11 daya during the teat uaing the bullunici~l puap and dilctlarge ayatbull already in uae at the well The well waa puaped at a atudy rate of 400 g- throughout the duration of the teat Puaped water waa uaecl by the aunicipali ty or diacharged through tire hydranta located outaide the area of influence of the teat Water l8vel Maaurnta were obtained fr011 a total of 22 vella

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and 2 piezoaetera durinq the teat Most observation wells werescrHned in the glacial drift aquifer however a few bedrockwells were also 110nitored to determine the deqree of hydraulicconnection between the qlacial drift and bedrock nov systemsRequhrly spaced readings were obtained from 13 wells withoccasional readinqa obtained from the reuininq 9 wells and 2piezometers Pressure tranaduceu and data lcqqers were used toobtain the reqularly spaced readinqs while manual measurementswere taken uainq an M-scopeo or popper in the wells whereoccasional readings were obtained The transducer readinqa wereverified daily by aupplental manual meaaureMnta Table 1lists the observations wells used durinq the teat and themeasurement technique used for each well For three days priorto tbe teat and throuqhout the duration at the teat backgroundwater level readings were obtained troa a well located outsidethe area of influence ot the teat (ERT-14) to provide data onbampckqround water level tluctuations At the conclusion ot~in9 activities water level recovery measur-nu wereobtained fro the observation velll tor a 2 day period todeteraine the rate of recovery of the vella back to equilibriuaIn addition to the bullaaur-nt of water levels in vella durinqthe pu~~pinq test surface water Uov rates were periodicallyMaaured in Arqilla Brook both upatreaa and downstreu of theStation 110 l well prior to and durin9 the -in9 teat TlleoeMampaur-nta were obtained ift an att-pt to quantify the rate ofatr- recharqe to the aquifer that occurred durinq the teat foriaclusioft in the puapiR9 test analysis At each atreaa now rateMaaurift9 atatioft the streaa was divided into several aegaentsaliqaed perpendicular to the Uov direction The crosa-sectioftalarea and flow velocity of each sepent were Masured durin9 eachMaaurnt round Area asurnts were ude with a tapewhile the Uow velocitiea were uaaured usift9 a rotatift9 currentMtlr A siRqle velocity Maaurnt vas obtained for eachatr SlfiMRt durinq each Maaurnt round The six-tenth bull 1 bulltbod vaa used to deterbulline the depth at which the velocityMasurftt was obtained (eix- tenth bulls of the total depth troathe ater aurface to the atreaa bottoa)

A n-r of velll were also aaapled prior to and idiatelyafter the CODCluaion of the puapinq teat in order to ideRtityany chaftqes in water quality due to the aquifer reapoftae to thepwapift9 of the Station No l well The samples were collectedusinCJ the Mthoda deser ibed in the Saapling and Analysis Plan andwere analyzed for volatile organica

The Station No l well vas alae aaapled twice per each 109 cycleof tiae durinCJ the pwapin9 teat These samples were analyzed forvolatile orCJanica metals and caon anions

W90029D -2shy

II

~ II

4 0 POIIPial TEST EIALOATIOR

Aa described previously water level measurements were obtainedfrobull 21 observation vella 2 piea011etera and the pumping well(Station No 1 well) during the pWIIping teat Data from 12 ofthe observation wella were utilized in determinin9 the aquifercharacteria tica of tranamhaivity hydraulic conductivity andstorativi ty The reJUininCJ 9 vella were not uaed i n thisanalyaia due to either a lack ot dravdown or because the well waascreened in a different aquifer (bedr ock) Due to wellinefficiency duwdovn meaaurementa i n the Station No 1 wellwere not factored into the analyaia Drawdown data from thep i eaoMtera were only uaed to determine the point at which t hevertical coaponent of groundwater nov became negliqible atpi ezQIHter well cluater locationbull P-6 110 and P-2112 A variety ot puapinq teat evaluation techniquebull were uaed in theanalyaia in order to provide a caprehenaive abullbullbullbullbullnt othydrQ9eol09ic conditione and to verity the reaulta obtainedtollowinq diacuaaion deacribea the pu8pin9 teat data reduction

Tbe and evaluation thoda aa well aa the teat reaulta

Prior to evalutint the teat data adjuatMnta had to be ude tothe raw tiM-drawdown data tor each well in order to ccpenaatefor varioua influencee All data thAt wae uaed Ma tiretcorrected for tread 10 that ainor fluctuationbull in water leveladue to precipitation bar011etric preaaura chantbullbullmiddot etc wouldnot be erroneoualy attributed to puapin9 operationa water levelcbaft9H in 110Ditorift9 well IIIT-14 were couideud to berepreeentative of natural fluctuationbull and were uaed to correctthe reatlin91 obtained fr011 the other obaervation vella Data fr011 aelected vella were alao corrected for dewaterin9lhh ia done to copenaate for the deerbullbullbullbull in the aaturatedthickneaa of the aquifer r11ultin9 fro puapin9 lhe correctionia neceaaary becauae tranaaiaaivity ia a function of the aquifer~~~cn~ =~==th~ ~uu~tt~~~=middot~~~~~ nen~l~1u~t1~ow~a~ lbull~t~ihwhen dravdowna exceed 10 of the initial aaturated thickneaa ofthe aquifer ror thia teat a aaewhat 110re ri9oroua andconaervative approach waa taken with correctionbull ude to dataf r oa all welll in which a dravdown of gtS of the initialaaturated thickneaa waa recorded durinq the teat Ota fromobaervation vella 1-50 110 and 112 required correction fordewaterinq uain9 an equation developed by Jacob (1944

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A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

W900290 __

The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

3 l

W90029D

DRUl PUMPING TST TCIIIIICAL MBIIORANDUM

SUPPLMDTAL - RI

GJ10VUAi1D IIULS SIT GROVaAJID MASSACIIUSTTS

- Corporation

IPA llork Aaaiv-nt No 04-lLll Contraot llo dl-tll-0117

Autuot 1990

rAIILB OP CQftDI8

Draft PullpiiiCJ raat ractmical -ralldbull Suppl-ntal - RIPS

Groveland Wellbull Site GrovelaDd llaecbuaetta

10 I~IOII bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull bullbullbull 1

zo - 30 -DQ Hft llftDICX(JGy bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull

40 -DQ Hft ampVAUIATIOII bullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull bullbullbullbull 41 Data Ra4uction bullbullbullbullbull bullbull bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull 4 2 Data Evaluation bullbullbullbullbullbullbullbullbullbull bullbull bullbull bull bullbullbullbullbullbullbullbull

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ID IWIHCUCOPCAPIUU- bullbullbullbullbullbullbullbullbullbullbullbullbullbullbull I

AIPDDII A - CALCIILAriOIII AIPDDII I - -Ill IOIL IMPLIS lllll

GRAil IIIZ AIALYIIB

10

Draft ~ing Teat Technical _randua Suppl-atal - RlPBGroveland Welle Site

Groveland Maaaachuaetta

I~IOII

Thil technical MatorandWD au-rhea the perforunce of EPA Work Alli9naent No 04-1L32 EPA Contract Nuaber 68-W8-0ll7 and evaluation of the puapin9 teat recently performed at the Groveland Wella Superfund Site alon9 with the related prelibullinary capture zone analyaia and dhcuaaiona and recoMndationa r~ardin9 upcoain9 data evaluation activitiea The teat waa conductecl aa part of the ManaC)-nt of Mi9ration I) RIPS that ia currently underway The raw data collected durin9 the tnt ia not included in thia aubllittal but will be included in the upcoain9 RI Report aubaittal rhe calculationbull perforeed for the analyaea are provided in Appendiz A

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r~fo~middot~~~f~~~~ bullt~0~t~ ~middot~~~9 t~idtfebullh~=~~tt ~te~tfehr~t~tcs drift aquif and to providbull a databaabull fr which to projbullct botb the current capture aone of the Station llo 1 wll aftd the capture aone of the well in the paat when it vaa puaped at a hiCJber rate tban the current rate Tile data waa alao to be uaed to recreate flow conditione in the paat when both the Station No 1 aDd Station llo 2 vella were in operation The 9oal of the capture aone analyaia ia to deterwine whether paat contination detectod in the ltatioa Ro 1 Hll could be relatod to thbull troundwater continant plUM centerecl around the Jlill PondJohnaon CrHk area fte followint eectiona deecribe the perfotunce of the _int teat data reduction and evaluation activitiea and tbe reaulta of the teet evaluation

lO _IS ftft -oGr

The Station No 1 well waa puaped continually for a period of 11 daya during the teat uaing the bullunici~l puap and dilctlarge ayatbull already in uae at the well The well waa puaped at a atudy rate of 400 g- throughout the duration of the teat Puaped water waa uaecl by the aunicipali ty or diacharged through tire hydranta located outaide the area of influence of the teat Water l8vel Maaurnta were obtained fr011 a total of 22 vella

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and 2 piezoaetera durinq the teat Most observation wells werescrHned in the glacial drift aquifer however a few bedrockwells were also 110nitored to determine the deqree of hydraulicconnection between the qlacial drift and bedrock nov systemsRequhrly spaced readings were obtained from 13 wells withoccasional readinqa obtained from the reuininq 9 wells and 2piezometers Pressure tranaduceu and data lcqqers were used toobtain the reqularly spaced readinqs while manual measurementswere taken uainq an M-scopeo or popper in the wells whereoccasional readings were obtained The transducer readinqa wereverified daily by aupplental manual meaaureMnta Table 1lists the observations wells used durinq the teat and themeasurement technique used for each well For three days priorto tbe teat and throuqhout the duration at the teat backgroundwater level readings were obtained troa a well located outsidethe area of influence ot the teat (ERT-14) to provide data onbampckqround water level tluctuations At the conclusion ot~in9 activities water level recovery measur-nu wereobtained fro the observation velll tor a 2 day period todeteraine the rate of recovery of the vella back to equilibriuaIn addition to the bullaaur-nt of water levels in vella durinqthe pu~~pinq test surface water Uov rates were periodicallyMaaured in Arqilla Brook both upatreaa and downstreu of theStation 110 l well prior to and durin9 the -in9 teat TlleoeMampaur-nta were obtained ift an att-pt to quantify the rate ofatr- recharqe to the aquifer that occurred durinq the teat foriaclusioft in the puapiR9 test analysis At each atreaa now rateMaaurift9 atatioft the streaa was divided into several aegaentsaliqaed perpendicular to the Uov direction The crosa-sectioftalarea and flow velocity of each sepent were Masured durin9 eachMaaurnt round Area asurnts were ude with a tapewhile the Uow velocitiea were uaaured usift9 a rotatift9 currentMtlr A siRqle velocity Maaurnt vas obtained for eachatr SlfiMRt durinq each Maaurnt round The six-tenth bull 1 bulltbod vaa used to deterbulline the depth at which the velocityMasurftt was obtained (eix- tenth bulls of the total depth troathe ater aurface to the atreaa bottoa)

A n-r of velll were also aaapled prior to and idiatelyafter the CODCluaion of the puapinq teat in order to ideRtityany chaftqes in water quality due to the aquifer reapoftae to thepwapift9 of the Station No l well The samples were collectedusinCJ the Mthoda deser ibed in the Saapling and Analysis Plan andwere analyzed for volatile organica

The Station No l well vas alae aaapled twice per each 109 cycleof tiae durinCJ the pwapin9 teat These samples were analyzed forvolatile orCJanica metals and caon anions

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II

~ II

4 0 POIIPial TEST EIALOATIOR

Aa described previously water level measurements were obtainedfrobull 21 observation vella 2 piea011etera and the pumping well(Station No 1 well) during the pWIIping teat Data from 12 ofthe observation wella were utilized in determinin9 the aquifercharacteria tica of tranamhaivity hydraulic conductivity andstorativi ty The reJUininCJ 9 vella were not uaed i n thisanalyaia due to either a lack ot dravdown or because the well waascreened in a different aquifer (bedr ock) Due to wellinefficiency duwdovn meaaurementa i n the Station No 1 wellwere not factored into the analyaia Drawdown data from thep i eaoMtera were only uaed to determine the point at which t hevertical coaponent of groundwater nov became negliqible atpi ezQIHter well cluater locationbull P-6 110 and P-2112 A variety ot puapinq teat evaluation techniquebull were uaed in theanalyaia in order to provide a caprehenaive abullbullbullbullbullnt othydrQ9eol09ic conditione and to verity the reaulta obtainedtollowinq diacuaaion deacribea the pu8pin9 teat data reduction

Tbe and evaluation thoda aa well aa the teat reaulta

Prior to evalutint the teat data adjuatMnta had to be ude tothe raw tiM-drawdown data tor each well in order to ccpenaatefor varioua influencee All data thAt wae uaed Ma tiretcorrected for tread 10 that ainor fluctuationbull in water leveladue to precipitation bar011etric preaaura chantbullbullmiddot etc wouldnot be erroneoualy attributed to puapin9 operationa water levelcbaft9H in 110Ditorift9 well IIIT-14 were couideud to berepreeentative of natural fluctuationbull and were uaed to correctthe reatlin91 obtained fr011 the other obaervation vella Data fr011 aelected vella were alao corrected for dewaterin9lhh ia done to copenaate for the deerbullbullbullbull in the aaturatedthickneaa of the aquifer r11ultin9 fro puapin9 lhe correctionia neceaaary becauae tranaaiaaivity ia a function of the aquifer~~~cn~ =~==th~ ~uu~tt~~~=middot~~~~~ nen~l~1u~t1~ow~a~ lbull~t~ihwhen dravdowna exceed 10 of the initial aaturated thickneaa ofthe aquifer ror thia teat a aaewhat 110re ri9oroua andconaervative approach waa taken with correctionbull ude to dataf r oa all welll in which a dravdown of gtS of the initialaaturated thickneaa waa recorded durinq the teat Ota fromobaervation vella 1-50 110 and 112 required correction fordewaterinq uain9 an equation developed by Jacob (1944

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A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

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The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

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Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

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II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

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DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

rAIILB OP CQftDI8

Draft PullpiiiCJ raat ractmical -ralldbull Suppl-ntal - RIPS

Groveland Wellbull Site GrovelaDd llaecbuaetta

10 I~IOII bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull bullbullbull 1

zo - 30 -DQ Hft llftDICX(JGy bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull

40 -DQ Hft ampVAUIATIOII bullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull bullbullbullbull 41 Data Ra4uction bullbullbullbullbull bullbull bullbullbullbullbullbullbullbullbullbullbullbullbullbullbullbull bull 4 2 Data Evaluation bullbullbullbullbullbullbullbullbullbull bullbull bullbull bull bullbullbullbullbullbullbullbull

sa -mg Hft a-n

ID IWIHCUCOPCAPIUU- bullbullbullbullbullbullbullbullbullbullbullbullbullbullbull I

AIPDDII A - CALCIILAriOIII AIPDDII I - -Ill IOIL IMPLIS lllll

GRAil IIIZ AIALYIIB

10

Draft ~ing Teat Technical _randua Suppl-atal - RlPBGroveland Welle Site

Groveland Maaaachuaetta

I~IOII

Thil technical MatorandWD au-rhea the perforunce of EPA Work Alli9naent No 04-1L32 EPA Contract Nuaber 68-W8-0ll7 and evaluation of the puapin9 teat recently performed at the Groveland Wella Superfund Site alon9 with the related prelibullinary capture zone analyaia and dhcuaaiona and recoMndationa r~ardin9 upcoain9 data evaluation activitiea The teat waa conductecl aa part of the ManaC)-nt of Mi9ration I) RIPS that ia currently underway The raw data collected durin9 the tnt ia not included in thia aubllittal but will be included in the upcoain9 RI Report aubaittal rhe calculationbull perforeed for the analyaea are provided in Appendiz A

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r~fo~middot~~~f~~~~ bullt~0~t~ ~middot~~~9 t~idtfebullh~=~~tt ~te~tfehr~t~tcs drift aquif and to providbull a databaabull fr which to projbullct botb the current capture aone of the Station llo 1 wll aftd the capture aone of the well in the paat when it vaa puaped at a hiCJber rate tban the current rate Tile data waa alao to be uaed to recreate flow conditione in the paat when both the Station No 1 aDd Station llo 2 vella were in operation The 9oal of the capture aone analyaia ia to deterwine whether paat contination detectod in the ltatioa Ro 1 Hll could be relatod to thbull troundwater continant plUM centerecl around the Jlill PondJohnaon CrHk area fte followint eectiona deecribe the perfotunce of the _int teat data reduction and evaluation activitiea and tbe reaulta of the teet evaluation

lO _IS ftft -oGr

The Station No 1 well waa puaped continually for a period of 11 daya during the teat uaing the bullunici~l puap and dilctlarge ayatbull already in uae at the well The well waa puaped at a atudy rate of 400 g- throughout the duration of the teat Puaped water waa uaecl by the aunicipali ty or diacharged through tire hydranta located outaide the area of influence of the teat Water l8vel Maaurnta were obtained fr011 a total of 22 vella

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and 2 piezoaetera durinq the teat Most observation wells werescrHned in the glacial drift aquifer however a few bedrockwells were also 110nitored to determine the deqree of hydraulicconnection between the qlacial drift and bedrock nov systemsRequhrly spaced readings were obtained from 13 wells withoccasional readinqa obtained from the reuininq 9 wells and 2piezometers Pressure tranaduceu and data lcqqers were used toobtain the reqularly spaced readinqs while manual measurementswere taken uainq an M-scopeo or popper in the wells whereoccasional readings were obtained The transducer readinqa wereverified daily by aupplental manual meaaureMnta Table 1lists the observations wells used durinq the teat and themeasurement technique used for each well For three days priorto tbe teat and throuqhout the duration at the teat backgroundwater level readings were obtained troa a well located outsidethe area of influence ot the teat (ERT-14) to provide data onbampckqround water level tluctuations At the conclusion ot~in9 activities water level recovery measur-nu wereobtained fro the observation velll tor a 2 day period todeteraine the rate of recovery of the vella back to equilibriuaIn addition to the bullaaur-nt of water levels in vella durinqthe pu~~pinq test surface water Uov rates were periodicallyMaaured in Arqilla Brook both upatreaa and downstreu of theStation 110 l well prior to and durin9 the -in9 teat TlleoeMampaur-nta were obtained ift an att-pt to quantify the rate ofatr- recharqe to the aquifer that occurred durinq the teat foriaclusioft in the puapiR9 test analysis At each atreaa now rateMaaurift9 atatioft the streaa was divided into several aegaentsaliqaed perpendicular to the Uov direction The crosa-sectioftalarea and flow velocity of each sepent were Masured durin9 eachMaaurnt round Area asurnts were ude with a tapewhile the Uow velocitiea were uaaured usift9 a rotatift9 currentMtlr A siRqle velocity Maaurnt vas obtained for eachatr SlfiMRt durinq each Maaurnt round The six-tenth bull 1 bulltbod vaa used to deterbulline the depth at which the velocityMasurftt was obtained (eix- tenth bulls of the total depth troathe ater aurface to the atreaa bottoa)

A n-r of velll were also aaapled prior to and idiatelyafter the CODCluaion of the puapinq teat in order to ideRtityany chaftqes in water quality due to the aquifer reapoftae to thepwapift9 of the Station No l well The samples were collectedusinCJ the Mthoda deser ibed in the Saapling and Analysis Plan andwere analyzed for volatile organica

The Station No l well vas alae aaapled twice per each 109 cycleof tiae durinCJ the pwapin9 teat These samples were analyzed forvolatile orCJanica metals and caon anions

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II

~ II

4 0 POIIPial TEST EIALOATIOR

Aa described previously water level measurements were obtainedfrobull 21 observation vella 2 piea011etera and the pumping well(Station No 1 well) during the pWIIping teat Data from 12 ofthe observation wella were utilized in determinin9 the aquifercharacteria tica of tranamhaivity hydraulic conductivity andstorativi ty The reJUininCJ 9 vella were not uaed i n thisanalyaia due to either a lack ot dravdown or because the well waascreened in a different aquifer (bedr ock) Due to wellinefficiency duwdovn meaaurementa i n the Station No 1 wellwere not factored into the analyaia Drawdown data from thep i eaoMtera were only uaed to determine the point at which t hevertical coaponent of groundwater nov became negliqible atpi ezQIHter well cluater locationbull P-6 110 and P-2112 A variety ot puapinq teat evaluation techniquebull were uaed in theanalyaia in order to provide a caprehenaive abullbullbullbullbullnt othydrQ9eol09ic conditione and to verity the reaulta obtainedtollowinq diacuaaion deacribea the pu8pin9 teat data reduction

Tbe and evaluation thoda aa well aa the teat reaulta

Prior to evalutint the teat data adjuatMnta had to be ude tothe raw tiM-drawdown data tor each well in order to ccpenaatefor varioua influencee All data thAt wae uaed Ma tiretcorrected for tread 10 that ainor fluctuationbull in water leveladue to precipitation bar011etric preaaura chantbullbullmiddot etc wouldnot be erroneoualy attributed to puapin9 operationa water levelcbaft9H in 110Ditorift9 well IIIT-14 were couideud to berepreeentative of natural fluctuationbull and were uaed to correctthe reatlin91 obtained fr011 the other obaervation vella Data fr011 aelected vella were alao corrected for dewaterin9lhh ia done to copenaate for the deerbullbullbullbull in the aaturatedthickneaa of the aquifer r11ultin9 fro puapin9 lhe correctionia neceaaary becauae tranaaiaaivity ia a function of the aquifer~~~cn~ =~==th~ ~uu~tt~~~=middot~~~~~ nen~l~1u~t1~ow~a~ lbull~t~ihwhen dravdowna exceed 10 of the initial aaturated thickneaa ofthe aquifer ror thia teat a aaewhat 110re ri9oroua andconaervative approach waa taken with correctionbull ude to dataf r oa all welll in which a dravdown of gtS of the initialaaturated thickneaa waa recorded durinq the teat Ota fromobaervation vella 1-50 110 and 112 required correction fordewaterinq uain9 an equation developed by Jacob (1944

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A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

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The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

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Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

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II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

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DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

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10

Draft ~ing Teat Technical _randua Suppl-atal - RlPBGroveland Welle Site

Groveland Maaaachuaetta

I~IOII

Thil technical MatorandWD au-rhea the perforunce of EPA Work Alli9naent No 04-1L32 EPA Contract Nuaber 68-W8-0ll7 and evaluation of the puapin9 teat recently performed at the Groveland Wella Superfund Site alon9 with the related prelibullinary capture zone analyaia and dhcuaaiona and recoMndationa r~ardin9 upcoain9 data evaluation activitiea The teat waa conductecl aa part of the ManaC)-nt of Mi9ration I) RIPS that ia currently underway The raw data collected durin9 the tnt ia not included in thia aubllittal but will be included in the upcoain9 RI Report aubaittal rhe calculationbull perforeed for the analyaea are provided in Appendiz A

zo shy

r~fo~middot~~~f~~~~ bullt~0~t~ ~middot~~~9 t~idtfebullh~=~~tt ~te~tfehr~t~tcs drift aquif and to providbull a databaabull fr which to projbullct botb the current capture aone of the Station llo 1 wll aftd the capture aone of the well in the paat when it vaa puaped at a hiCJber rate tban the current rate Tile data waa alao to be uaed to recreate flow conditione in the paat when both the Station No 1 aDd Station llo 2 vella were in operation The 9oal of the capture aone analyaia ia to deterwine whether paat contination detectod in the ltatioa Ro 1 Hll could be relatod to thbull troundwater continant plUM centerecl around the Jlill PondJohnaon CrHk area fte followint eectiona deecribe the perfotunce of the _int teat data reduction and evaluation activitiea and tbe reaulta of the teet evaluation

lO _IS ftft -oGr

The Station No 1 well waa puaped continually for a period of 11 daya during the teat uaing the bullunici~l puap and dilctlarge ayatbull already in uae at the well The well waa puaped at a atudy rate of 400 g- throughout the duration of the teat Puaped water waa uaecl by the aunicipali ty or diacharged through tire hydranta located outaide the area of influence of the teat Water l8vel Maaurnta were obtained fr011 a total of 22 vella

W90029D -1shy

and 2 piezoaetera durinq the teat Most observation wells werescrHned in the glacial drift aquifer however a few bedrockwells were also 110nitored to determine the deqree of hydraulicconnection between the qlacial drift and bedrock nov systemsRequhrly spaced readings were obtained from 13 wells withoccasional readinqa obtained from the reuininq 9 wells and 2piezometers Pressure tranaduceu and data lcqqers were used toobtain the reqularly spaced readinqs while manual measurementswere taken uainq an M-scopeo or popper in the wells whereoccasional readings were obtained The transducer readinqa wereverified daily by aupplental manual meaaureMnta Table 1lists the observations wells used durinq the teat and themeasurement technique used for each well For three days priorto tbe teat and throuqhout the duration at the teat backgroundwater level readings were obtained troa a well located outsidethe area of influence ot the teat (ERT-14) to provide data onbampckqround water level tluctuations At the conclusion ot~in9 activities water level recovery measur-nu wereobtained fro the observation velll tor a 2 day period todeteraine the rate of recovery of the vella back to equilibriuaIn addition to the bullaaur-nt of water levels in vella durinqthe pu~~pinq test surface water Uov rates were periodicallyMaaured in Arqilla Brook both upatreaa and downstreu of theStation 110 l well prior to and durin9 the -in9 teat TlleoeMampaur-nta were obtained ift an att-pt to quantify the rate ofatr- recharqe to the aquifer that occurred durinq the teat foriaclusioft in the puapiR9 test analysis At each atreaa now rateMaaurift9 atatioft the streaa was divided into several aegaentsaliqaed perpendicular to the Uov direction The crosa-sectioftalarea and flow velocity of each sepent were Masured durin9 eachMaaurnt round Area asurnts were ude with a tapewhile the Uow velocitiea were uaaured usift9 a rotatift9 currentMtlr A siRqle velocity Maaurnt vas obtained for eachatr SlfiMRt durinq each Maaurnt round The six-tenth bull 1 bulltbod vaa used to deterbulline the depth at which the velocityMasurftt was obtained (eix- tenth bulls of the total depth troathe ater aurface to the atreaa bottoa)

A n-r of velll were also aaapled prior to and idiatelyafter the CODCluaion of the puapinq teat in order to ideRtityany chaftqes in water quality due to the aquifer reapoftae to thepwapift9 of the Station No l well The samples were collectedusinCJ the Mthoda deser ibed in the Saapling and Analysis Plan andwere analyzed for volatile organica

The Station No l well vas alae aaapled twice per each 109 cycleof tiae durinCJ the pwapin9 teat These samples were analyzed forvolatile orCJanica metals and caon anions

W90029D -2shy

II

~ II

4 0 POIIPial TEST EIALOATIOR

Aa described previously water level measurements were obtainedfrobull 21 observation vella 2 piea011etera and the pumping well(Station No 1 well) during the pWIIping teat Data from 12 ofthe observation wella were utilized in determinin9 the aquifercharacteria tica of tranamhaivity hydraulic conductivity andstorativi ty The reJUininCJ 9 vella were not uaed i n thisanalyaia due to either a lack ot dravdown or because the well waascreened in a different aquifer (bedr ock) Due to wellinefficiency duwdovn meaaurementa i n the Station No 1 wellwere not factored into the analyaia Drawdown data from thep i eaoMtera were only uaed to determine the point at which t hevertical coaponent of groundwater nov became negliqible atpi ezQIHter well cluater locationbull P-6 110 and P-2112 A variety ot puapinq teat evaluation techniquebull were uaed in theanalyaia in order to provide a caprehenaive abullbullbullbullbullnt othydrQ9eol09ic conditione and to verity the reaulta obtainedtollowinq diacuaaion deacribea the pu8pin9 teat data reduction

Tbe and evaluation thoda aa well aa the teat reaulta

Prior to evalutint the teat data adjuatMnta had to be ude tothe raw tiM-drawdown data tor each well in order to ccpenaatefor varioua influencee All data thAt wae uaed Ma tiretcorrected for tread 10 that ainor fluctuationbull in water leveladue to precipitation bar011etric preaaura chantbullbullmiddot etc wouldnot be erroneoualy attributed to puapin9 operationa water levelcbaft9H in 110Ditorift9 well IIIT-14 were couideud to berepreeentative of natural fluctuationbull and were uaed to correctthe reatlin91 obtained fr011 the other obaervation vella Data fr011 aelected vella were alao corrected for dewaterin9lhh ia done to copenaate for the deerbullbullbullbull in the aaturatedthickneaa of the aquifer r11ultin9 fro puapin9 lhe correctionia neceaaary becauae tranaaiaaivity ia a function of the aquifer~~~cn~ =~==th~ ~uu~tt~~~=middot~~~~~ nen~l~1u~t1~ow~a~ lbull~t~ihwhen dravdowna exceed 10 of the initial aaturated thickneaa ofthe aquifer ror thia teat a aaewhat 110re ri9oroua andconaervative approach waa taken with correctionbull ude to dataf r oa all welll in which a dravdown of gtS of the initialaaturated thickneaa waa recorded durinq the teat Ota fromobaervation vella 1-50 110 and 112 required correction fordewaterinq uain9 an equation developed by Jacob (1944

W90029D -l shy

A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

W900290 __

The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

and 2 piezoaetera durinq the teat Most observation wells werescrHned in the glacial drift aquifer however a few bedrockwells were also 110nitored to determine the deqree of hydraulicconnection between the qlacial drift and bedrock nov systemsRequhrly spaced readings were obtained from 13 wells withoccasional readinqa obtained from the reuininq 9 wells and 2piezometers Pressure tranaduceu and data lcqqers were used toobtain the reqularly spaced readinqs while manual measurementswere taken uainq an M-scopeo or popper in the wells whereoccasional readings were obtained The transducer readinqa wereverified daily by aupplental manual meaaureMnta Table 1lists the observations wells used durinq the teat and themeasurement technique used for each well For three days priorto tbe teat and throuqhout the duration at the teat backgroundwater level readings were obtained troa a well located outsidethe area of influence ot the teat (ERT-14) to provide data onbampckqround water level tluctuations At the conclusion ot~in9 activities water level recovery measur-nu wereobtained fro the observation velll tor a 2 day period todeteraine the rate of recovery of the vella back to equilibriuaIn addition to the bullaaur-nt of water levels in vella durinqthe pu~~pinq test surface water Uov rates were periodicallyMaaured in Arqilla Brook both upatreaa and downstreu of theStation 110 l well prior to and durin9 the -in9 teat TlleoeMampaur-nta were obtained ift an att-pt to quantify the rate ofatr- recharqe to the aquifer that occurred durinq the teat foriaclusioft in the puapiR9 test analysis At each atreaa now rateMaaurift9 atatioft the streaa was divided into several aegaentsaliqaed perpendicular to the Uov direction The crosa-sectioftalarea and flow velocity of each sepent were Masured durin9 eachMaaurnt round Area asurnts were ude with a tapewhile the Uow velocitiea were uaaured usift9 a rotatift9 currentMtlr A siRqle velocity Maaurnt vas obtained for eachatr SlfiMRt durinq each Maaurnt round The six-tenth bull 1 bulltbod vaa used to deterbulline the depth at which the velocityMasurftt was obtained (eix- tenth bulls of the total depth troathe ater aurface to the atreaa bottoa)

A n-r of velll were also aaapled prior to and idiatelyafter the CODCluaion of the puapinq teat in order to ideRtityany chaftqes in water quality due to the aquifer reapoftae to thepwapift9 of the Station No l well The samples were collectedusinCJ the Mthoda deser ibed in the Saapling and Analysis Plan andwere analyzed for volatile organica

The Station No l well vas alae aaapled twice per each 109 cycleof tiae durinCJ the pwapin9 teat These samples were analyzed forvolatile orCJanica metals and caon anions

W90029D -2shy

II

~ II

4 0 POIIPial TEST EIALOATIOR

Aa described previously water level measurements were obtainedfrobull 21 observation vella 2 piea011etera and the pumping well(Station No 1 well) during the pWIIping teat Data from 12 ofthe observation wella were utilized in determinin9 the aquifercharacteria tica of tranamhaivity hydraulic conductivity andstorativi ty The reJUininCJ 9 vella were not uaed i n thisanalyaia due to either a lack ot dravdown or because the well waascreened in a different aquifer (bedr ock) Due to wellinefficiency duwdovn meaaurementa i n the Station No 1 wellwere not factored into the analyaia Drawdown data from thep i eaoMtera were only uaed to determine the point at which t hevertical coaponent of groundwater nov became negliqible atpi ezQIHter well cluater locationbull P-6 110 and P-2112 A variety ot puapinq teat evaluation techniquebull were uaed in theanalyaia in order to provide a caprehenaive abullbullbullbullbullnt othydrQ9eol09ic conditione and to verity the reaulta obtainedtollowinq diacuaaion deacribea the pu8pin9 teat data reduction

Tbe and evaluation thoda aa well aa the teat reaulta

Prior to evalutint the teat data adjuatMnta had to be ude tothe raw tiM-drawdown data tor each well in order to ccpenaatefor varioua influencee All data thAt wae uaed Ma tiretcorrected for tread 10 that ainor fluctuationbull in water leveladue to precipitation bar011etric preaaura chantbullbullmiddot etc wouldnot be erroneoualy attributed to puapin9 operationa water levelcbaft9H in 110Ditorift9 well IIIT-14 were couideud to berepreeentative of natural fluctuationbull and were uaed to correctthe reatlin91 obtained fr011 the other obaervation vella Data fr011 aelected vella were alao corrected for dewaterin9lhh ia done to copenaate for the deerbullbullbullbull in the aaturatedthickneaa of the aquifer r11ultin9 fro puapin9 lhe correctionia neceaaary becauae tranaaiaaivity ia a function of the aquifer~~~cn~ =~==th~ ~uu~tt~~~=middot~~~~~ nen~l~1u~t1~ow~a~ lbull~t~ihwhen dravdowna exceed 10 of the initial aaturated thickneaa ofthe aquifer ror thia teat a aaewhat 110re ri9oroua andconaervative approach waa taken with correctionbull ude to dataf r oa all welll in which a dravdown of gtS of the initialaaturated thickneaa waa recorded durinq the teat Ota fromobaervation vella 1-50 110 and 112 required correction fordewaterinq uain9 an equation developed by Jacob (1944

W90029D -l shy

A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

W900290 __

The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

II

~ II

4 0 POIIPial TEST EIALOATIOR

Aa described previously water level measurements were obtainedfrobull 21 observation vella 2 piea011etera and the pumping well(Station No 1 well) during the pWIIping teat Data from 12 ofthe observation wella were utilized in determinin9 the aquifercharacteria tica of tranamhaivity hydraulic conductivity andstorativi ty The reJUininCJ 9 vella were not uaed i n thisanalyaia due to either a lack ot dravdown or because the well waascreened in a different aquifer (bedr ock) Due to wellinefficiency duwdovn meaaurementa i n the Station No 1 wellwere not factored into the analyaia Drawdown data from thep i eaoMtera were only uaed to determine the point at which t hevertical coaponent of groundwater nov became negliqible atpi ezQIHter well cluater locationbull P-6 110 and P-2112 A variety ot puapinq teat evaluation techniquebull were uaed in theanalyaia in order to provide a caprehenaive abullbullbullbullbullnt othydrQ9eol09ic conditione and to verity the reaulta obtainedtollowinq diacuaaion deacribea the pu8pin9 teat data reduction

Tbe and evaluation thoda aa well aa the teat reaulta

Prior to evalutint the teat data adjuatMnta had to be ude tothe raw tiM-drawdown data tor each well in order to ccpenaatefor varioua influencee All data thAt wae uaed Ma tiretcorrected for tread 10 that ainor fluctuationbull in water leveladue to precipitation bar011etric preaaura chantbullbullmiddot etc wouldnot be erroneoualy attributed to puapin9 operationa water levelcbaft9H in 110Ditorift9 well IIIT-14 were couideud to berepreeentative of natural fluctuationbull and were uaed to correctthe reatlin91 obtained fr011 the other obaervation vella Data fr011 aelected vella were alao corrected for dewaterin9lhh ia done to copenaate for the deerbullbullbullbull in the aaturatedthickneaa of the aquifer r11ultin9 fro puapin9 lhe correctionia neceaaary becauae tranaaiaaivity ia a function of the aquifer~~~cn~ =~==th~ ~uu~tt~~~=middot~~~~~ nen~l~1u~t1~ow~a~ lbull~t~ihwhen dravdowna exceed 10 of the initial aaturated thickneaa ofthe aquifer ror thia teat a aaewhat 110re ri9oroua andconaervative approach waa taken with correctionbull ude to dataf r oa all welll in which a dravdown of gtS of the initialaaturated thickneaa waa recorded durinq the teat Ota fromobaervation vella 1-50 110 and 112 required correction fordewaterinq uain9 an equation developed by Jacob (1944

W90029D -l shy

A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

W900290 __

The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

A correction factor for partial penetration vas also appliedwhere appropriate Partial penetration effects occur when thepumping andor observation wells are screened or open over onlypart of the aquifer being pumped These effects are a reflectionof vertical groundwater flow components resulting from pumpi ngThe eftects decrease with increasing distance between the pumpingand observation well and with increasing time For the Grove l andWelh puaping teat corrections for partial penetration were onlyrequired for observation well l-50 Corrections were notrequired for the remaining wells as t hey were located far enoughfro the pWiping well that the vertical component of groundwaterflow resulting trOll pumpinc was neqliqible Drawdown data t orclueter locations P-6llO and P-2 112 revealed that within ashort tiM period after pUIIpinq was started the meaeureddravdowne at the top and bottom of the aquifer were virtually thes This indicates that verticAl flow within the Aquifer ianegligible at these diltancee frobull the pumping well as well asany 9reater distancebull The drawdown data for l-50 vas correctedfor partial penetration ueinq equations presented in Walton(1914) bullbull developed by Bantuah (1964)

bulla Data IYaluatloa

~~eiraroel~~er=~~en~t~ baaedoft uainq several techniques yield re reliable results thananalyses that are baaed Oft a ainqle evaluation Mthod Thetectuaiques selected are all applicable to an unconfined aquifer lach Mthod used cUtten aoaewbat froa the other aethoda relativer~tns~rbullo~e~~~clO~bullc~~~n~ seach Mthod provides a related but different perspective of theteat

lbe corrected ti-drawdovn data for observation velll 1-SO 110112 111 115 11083 NUllA ERTll ERT2 No 3 and 114 wereplotted Individually on both lOCJ-lOCJ and al-lOCJ (with time onthe log axla) qrapb pa-r ror the loq-loq plots type curveutcbinq tecbaiquea were -played to deteraine aquifercharacteristics Several seta of type curves were used in theanalysis aa no one sat of type curvebull vas founc to beAppropriate for all of the data plots Curve tching thniquesdeveloped for unconfined aquifers by Boulton (1963 or Stallun( 1965) were applied aa necessary depending on which methodprovided a beat fit with each data set Tranaaiaaivity (T) andatorativity (I) were calculated directly fr011 each IHthod Theratio of horhontal to vertical hydrAulic conductivity (kh Kv)waa deterbullined directly through Stallmans method whileBoulton 1 Mthod vas aoditied throuqh a conversion developed byNelllan (1975) to deteraine the IChKv utio

W900290 __

The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

The semi-log timedravdown data plots were evaluated using amethod developed by Cooper and JAcob (1946) Thil AnAlysistechnique 11 uaed to determine T and s and cAn Alae be uaed toidentity Any boundAry conditionbull thAt are preaent In additionto evAluating timedrAwdown dAta drawdown meaaurementa atvarying diatancea frobull the puaping well at a qiven time after thestart of puapin9 were AnAlyzed to determine aquifercharActer iatica Thia me thad also developed by Cooper and JAcob(1946) conaiata of plotting diatance-drawdown dAtA on a aemi-loqqrAptl (diatance on the loq uia) to qenerate estiutea of T ands Boundary conditionbull cAn alao be identified using thia methodA total of 12 observAtion vella were uaed in thia anAlylia tinAl check An Analyah of inward flow throuqh ttle Area of aAa a

cylinder of variable heiqtlt to A puapinq well waa perforaed tofactor in to the Analyaia the varyinq aquifer thickneaa whichexiata in the Area aurroundinq the Station No 1 well Theperiaeter of a cylinder with A radiua defined by the distancefr011 the ~in9 well to the point where the 9radient induced bypw~pin9 equals an aaai9ned value (in this case 005 waa choaen)ia coabined with the avera9e Aquifer thickneaa alon9 ttleperiMter to deteraine the area of croaa-aectional flow Thiaarea (A) aloruJ with the assi9nft gracHent (i) and the teat-in9 rate (Q) ia lnbull~rted Into Darcybull oquotion (QoliA) todeteraine the overall hydraulic conductivity of the aquiferaaterials

fte analysis of the streu flow data for Ar9Ula Brook waaanaly1ed by dividinCJ the croaa-aectional area of the atreu ateach nov Masur-nt atation into diacrete areaa correapondinCJto bullcb of tbe aebulleral Masur inCJ pointa located acroaa the widthof tbe atreu at tbat station The aeasured flow velocity foreach aeasuring point waa aultiplied by the correapondinCJ area to~ner~ ~==r~rf~ = =~tht~n~ti~=ewere added tQCJether to deteraine the total volUMtrlc flowvelocity for that station

50 -~~~~~--Water levels were steadily drawn down throuq~bout the courae ofthe papin9 teat in 110at vella At the end of the 11 days ofptmpinq~ there were no indications that ateady-atate conditionbull(no furttler drawdown) were bein9 approached This indicates thatdurinCJ the ti period of the teat recharve to the aquiter(throuCJh precipitation aurface water infiltration etc) waaliaited within the cone of depression and waa not enou9h toottaet the withdrawal tAte (400 en-) Baaed on thh it can beasauaed that the cone or depreaaion would continue to expand itpuapinCJ were to be continued beyond ll daya W90029D -5shy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

Baaed on the obaerved pattern of drawdowna in the aquifersurroundin9 the Station No 1 well there appeara to be a slighttrend of preferential drawdown to the southweat towards MillPond The aone of preferential drawdown correspondbull roughly tothe axia of the buried valley Conversely very little dravdownwaa meaaured weat of Main Street near the Station No 2 wellrelative to dravdowna equidiatant to Station No 2 in otherdirections frobull the Stationot drawdovn h No l well The reason tor this lacknot apparent but may be due to the presence of alarge hill in thia area poaaibly creating a localized groundwatermounding condition

Significant dravdovna were obaerved in bedrock wella locatedwithin the area of influence of the teat The aaured drawdownawere alightly leaa than the drawdovna meaaured in adjacentoverburden vella The obaerved drawdowna are an indication thatthe bedrock groundwater nov syat h in good hydraulicc~nication with the overlying atratitiecl drift aquiferThe reaulta of the puaping teat evaluation are preaented in Table2 The tranaaiaaivityl atorativity and hydraulic conductivityvaluea generated tbrou9h the var ioua aDAlyail Mthoda are in9eneral atrnt with each other 1apparent althou9h bull~ differencebull areBatitea of aquifer traniaaivity and atorativitywere tbullnerally in good atrnt for the lOCJ-109 and bullbulli lOCJtibull-dravdown analJbullbullbull for each ob8ervatlon well There waa ageneral trend obaerved of increaain9 tranuiaaivity valuea forwella alitned with the puaping well at greater anglea to ArgUlaBrook in ~riaon to tboae wella ali9ned with the puapin9 wellin a direction parallel to the brook Obaervatlon wella 1-50112 1 aDd 111 2 are aligned parallel to the brook and had theloweat tranaaiaaivitiea~ baaed on the tiM-drawclown dataconveraely obaervation welll 111 115 and NOS l 1 located acro11and at an angle to the brook have the hiqheat tranaaiaaivitleabaaed Oft tbe ti-drawdown data Thia trend uy be related toone or both of two factora A recharging atreaa createa abouDdary coftditlon that ia dravdowna on the oppoaite aide ofthe atr fra the pw~ping well are decreaaed due to theinfiltration of water fr011 the atreaa to the aquifer Thhreaulta in an artificially hiqh calculated tranaai11ivity Theob11rvation vella located on a line parallel to the atreaa arealao located along the axil of a burieci bedrock valley a1 ibull thepuapiDg Will Thill well1 are all acreened near the ~bulle of theaquifer and aince the puapinq well 11 bullcreened over only thebotta 15 feet of the aquifer it aay preferentially draw vaterfra the d11p aediaenta within the buried valley Thibull couldgenerate increaaed drawdovn1 at depth alonq the valley axisrelative to other areaa and re1ult in lower calculated valuebull ottranaaialivity

11900290 -6shy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

Transmissivity values derived from the diatance-drawdown analysisshow a different trend The wells aligned parallel to the streamhave a higher tranamiaaivity thanthe stream those aligned at an angle toThis result is more consistent with expectedresults baaed on aquiter thickness data and geologiccleacr iptiona from boring logs Baaed on Walton (1987) in asituation where a stream acts as a source of recharge the mostreliable estiJUte of T is clerived frobull a distance-drawdownanalysia using observation wells aligned parallel to therecharging stream AI a result the results of thediatance-dravdown analysis for wells 1-so 110 112 and ERT 2are considered moat representative of the overall aquifer T andK It should be noted that the aquifer transmissivity will varyacross the study area due to the variations in aquifer thicknessthat occur

The supplental pumping teat anAlysis pertoraed using anassigned puaping-induced qradient the resulting periMter lengthof the equigradient contour and the aquifer thickness alonq theequigradient line was used to factor in the variations in aquiferthickness and the atreaa recharge into the teat analysis ThisMthod also allows tor all nearby vella to be used in the analyeis instead of analy1ing the well data individually or inseveral groupings AI can be aHn in Table z the results ofthis analysis capare wll with the ll derived troa thedietance-dravdown analysis verifying the representativeness ofthe results obtained troa each of the two Mthoda An overallaverage ll of about 90 ftday is considered to be representativeof the aquifer baaed on the puaping teat results Since thethickness of the atratiUed drift aquifer varies substantially~~1~~~he~rlr~gt=a~r~a1~~i ~~1r~3ayUsing the loq-loq type curve utching techniques the ratio ofthe horilontal versus vertical hydraulic conductivity (llhKv) ofthe aquifer sediMnta vas deterbullined An overall average KhKvratio of approalaately lOzl was eatabliabed using tbe data froaobserVation wells 1-so 110 llZ Eltr-Z N03 and llt ltle dAtatroa the observation vella located north of Argilla Brook was notincluded in this deterbullination Much higher horilontal tovertical ratios tor hydraulic conductivity were generated usingthe dAta troa these vella however the aquifer is underlocalized bullbulli- confined conditionsin the anouloualy hi9h ratio

in this area which resultsAI the analysis Uchnique usedaaaume1 unconfined conditionathe ratios calculated for thesevella are invalid and cannot be used lhe 101 ratio of Khltv isreasonable tor an aquifer of this type and correspondbull totypical KhKv ranges reported in published references

W900290 -7shy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

II

II

Aquifer storativity values generated from the pumping test datavaried from well to well With the exception of one well allvalues were leas than 15 averaging approximately 08 to 10 The calculated stontivitles generally fall within the lowerrange of typicAl storativity values for unconfined granularaquifers

No decrease in streAm flow rate from the upstream meaaur ingstation to the downstream station was measured in Argilla Brookduring the pumping teat Some streu recharge to the aquifer wasexpected during the test as the sand and gravel streu bed andapparent hydraulic connection between the stream and the aquifer(as evidenced by the water table contour mapa) both suggest thatstreu infiltration could readily occur during times middotwhen theaquifer is drawn down below the stream level The lAck of streamdepletion uy be a reflection of the ground thaw that occurredduring the test which would recharge the streu and maak anyinfiltration of water fr011 the strau to the aquifer Despitethis lack of Masurable 1treu infiltration it is likely that atlealt 101M inUltration occun during periods of extendedpuapibull9middot

The discharge of groundwater fro bedrock to the glacial driftaquifer during the puaping test as evidenced by the aignificantdravdowns noted in becSrock wells and the expected (although notverified) 1treu recharge to the aquifer during pwaping Act topartially counteract the paping-induced drawdown of thestratified drift aquifer ttlia resultl in sOIIeWhat leaaerdravdovna within the aquifer than would otherwile occur andultiutely reeults in slightly overestiaatad values of T and KActual T and I valuebull for the stratified drift sediMntl areprobably 10 to 20 percent lower than the calculated valuea 60 PIIOJKriOIIS OP CAPrUU ZOBI

The capture tones re1ultlng froa puaping the Station No 1 wellat both the current extraction rate of 400 gpa and the historicrate of 500 9P1 were projactecl froa the re1ults of the pwapinc)test middot lbe capture aone liai t vaa deterbullined both in theUP9radient (Iouth) direction fr011 the Station No 1 vall andalong Argilla Brook axtendinv froa the Station No 1 wall to thewalt towardbull Johnson Creak lhe upqradient capture 10ne limitvaa aatiaatad ualng a lllOdlticAtion of the standard technique ofdeteraining capture 1onea for vella in a uniform flow field(Bear 1979) The basic technique used a1sumea that all wAterextracted orivinatea fr011 the 1aae single upgradiant direction An adjustunt vbullbull required for thla analysis due to thetwo-directional flow or qroundvater thbullt occurs in the vicinityof the StAtion No 1 vall AI a ra1ult or 9roundvater discharge toArgilla Brook from both the north and south This vas factored W900290 -ashy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

into the analyta by partitioning the total nov into twocomponents one originating from the south and one from thenorth Two-thirds of the total well discharge wa1 Allwaed tooriginate fr011 the south AI the aquifer is thicker in thisdirection and the regional flow gradient is from the south to t henorth In addition to the above a1swaption an aquifer hydraulicconductivity of 90 ftday an average aquifer thickne11 of 60feet and an average groundwater flow gradient of 0068 (derivedfrom the groundwater contourmiddot map baaed on water levels taken t heday preceding the start of the pumping teat) were uaed tor theanalyail Baaed on the above apprcnch the eatimated capturezone width in the area south of Station No 1 il about 1400 teettor a pumping rate of 400 gp~ and 2100 teet tor a puapinq rate of600 qps Theae capture zone widtha would extend equidistant tothe eaat and weat trcxa a line drawn aouth troa the Station No 1well parallel to the groundwater now direction in the areaaouth of Station No 1

The extent of the capture zone ot the Station No l well in aveaterly direction alonq Arqilla Brook waa alao eatiaatedreaultl of the diatance-drawdown analyaia pepoundformed tor the The

pw~pin9 teat were uaed in thia projection aa thil datarepreaenta actual Maaured drawdovna in the aquifer in reaponaeto pw~pin9 Data troa wella 1-50 110 112 and ERT- 2 were uaedin thia analyaia aa theae welll are located alon9 a lineparallel to Ar9Ula Brook extendin9 we1t of the Station Mo 1=~~1~~~n~r=t~d~t~r1~=nf~~n~h 1~~oult1n9deribulled frca the pu11pin9 teat data at tbull15000 bullinutea (durin9 thelaat clay of pa~pin9) the capture aone of the Station No 1 well~1hr-rt 4 C ~=~~~~I t1~r1~uaed to find the dhtance tr011 tbe pw~pin9 well to where thepw~pinCJ-induced gradient equaled the Maaured atre 9radient of00033 A dlota of 556 fHt to tha t wao calculated bullbull thecapture aone llait alon9 Ar9illa Brook The capture aone Hbullitat 00 CJPII waa eatiuted by increaain9 the pmpin9 teat-projecteddrawrdown at tbe ltation Mo 1 well by 50 (Iince the puapin9 rateia iaCreaaed 50 obuller the rate uaed tor the pu11pin9 teat) bull A new1lope to tbe 41atance-drawdown line waa then deterbullined u1in9the Jacob equation tor the hi9ber pu8pin9 rate A new equationwaa then developed to repreaent thil line uainq the approach bullbull waa uaed tor the auppleMntal puapin9 teat analyaildeacribed previoualy Solvin9 to find the diatance where thepuapinq-induced 9tadilnt equall 0033 (AI above) a capture 1oneUbullit of about 140 teet to the weat alon9 Ar9illa Brook waadetenained

W900290 -9shy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

DIIAPT The effects of aquifer dewatering were ignored in theseevaluations to provide a conservative estimate of drawdownlevels In nality the additional dewater i ng of the aquifershould result in slightly greater drawdowns and capture zonelimits than are projected here

The projected historic capture zone due to the pumping of the~~=~=~=~~i~yw~~l~ ~5~~~~~~~9w ~=~~~~ ~~~~~ anaverage aquifer hydraulic conductivity of 90 ft day and anaverage aquifer thickness in the area around the Station No 2well of about 55 feet Aa described previoualy the K value of90 ftday ia baaed on data that il probably intluenced to somedeqree by streaa and bedrock ncharge to the stratified driftaquifer It ia valid to uae thil It value however because anyrecftarqe that occun under puapinq conditions h autoaaticallyfactored into the capture zone analyaia by uainq the unadjustedK which reaulta in an accurate representAtion of the actualaquifer reaponae to puapin9 A hiatoric pwapinq rate of 450 enshyand an overall now qradient of 0 0068 (aa waa uaecl for theStation No 1 analylia were alao uaed in the evaluationSlailar to Station No 1 qroundwater flova tovard1 the Station110 2 vicinity troa acne than a 1in9le direction under naturalconclitiona The r~~q~ional now pattern il fra 1outh to northwbile there ia alao localhed flow fra the veat and northeaattowarda the confluence of Ar9illa lrook and John1on Creekre1ult the total flow to the well va1 partitioned with 50

Aaof

athe flow aa1i9ned to the r~~q~ional flow pattern 25 a11iqned tonov trOll the veat and 25 troa the northeast The approxiuteeztent of the capture zone to the 1outh vaa calculated in aaiallar unner aa waa done tor the Station No 1 well Thereaultil9 capture sone width ia approxiutely 1300 feet centeredalon9 Johnaon CrHk and eztendin9 equidiatant to the eaat andweat ftlia capture aone would extend 1outhvard throu9h the MillPanel area

The ruulta of thil prelibullinary capture zone analyail indicatethat tbe conuaiution in the Mill Pond area 11 within thehiatoHc capt1are aone of the Station No 2 well The captureaone of the ltatlon No 1 well at the hl1toric pu~~ping rate of600 91111 ezteDIIa aouth to near and poaaibly within the outlyinqarea of the coatuinant pluae At the current extraction rate of400 91111bull the Station No1 capture zone moat likely does notextend to the area of the contaainant plwu This preliainary analyah waa performed uainq techniquesdeveloped for h0110qeneoua unitorbull qroundwater flow fields Anatteapt vaa ude to factor sae of the unique conditions presentat the lite into the analyaia by modifying socae inputs andI aaauaptiona- The varbtion in aquifer thickneaa changes in flow W90029D -10shy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

gradients multiple groundwater tlow directions and the presence of local stre within the study area complicate the capture zone analyts and cannot be easily factored in to an analytical model As such the results presented here should be considered preliminary only and subject to revision as further data analysis occurs Groundwater IIOdeUng should be strongly considered tor use in the capture zone analyst as ~~ampny of the uncertainties of the analytical IIOdel can be addressed uaing an appropriate computer code such aa the USGS NOOPLON IIOdel This uy be prticularly i~rtant since the preliaiMry analysis ahovs the historic Station No l capture acne extending to near the ed9e of the current eatent ot the continant pluae

To aid in further evaluation grain size analyds ot geoloqic auplea previously collected h reco-nded The list ot saaplea recaended tor grain aile analysis is provided in Appendix a

N90029D -llshy

TAIU1OIUIVAliONWIWFOISTAflONNO 1

NWINGmTSUPPUMlNTAl MOM lllfS

GROVElAND WILLS ~TIGROVELAND MASSACHUSETTS

WELL NO FREQUENCY OF MEASUREMENT DISTANCE FROM

READINGSbull TECHNIQUEbullbull STATION NO I (h)

1-50 T so

110 T 128

112 T

111 T

200NUS3 T l4S

NUSJA T

JbullSbull115 T lSl

ERT II r soo

ERT2 T 617

lot 0 M 702

No T

bull 105 I bull

11 T 10

T 1000 bullNo17 0 M 1520

101 0 M 1520

101 0 M 1550

104 0 M 1750

NU54A 0 M 1710

ERT16 0 M 1780 ERTZ 0 M 1160

DIQl5 0 M 230 ERT1 T 2740

PieiOmettr$ P6 0 M Ill

P2 0 M 277

bull R bull Rc)ulariy obUiined reldingt0 bull Occasional ruclings

T bull Transducet M bull Manu-

TAILpound2PUMPIING TEST IIESULTS SUMMARY

SUPPLEMENTAL MOM IIIIFSGAOVELAND WEW STE

GROVELAND MASSAOIUSEnS

TIMEmiddotORAWOOWNbull DISTANCEmiddot ORAWOOWNbullbullWEll NO

T(ftl lday) K(ftldbully) s Tft11diy) K(ftdbull yl s

1-SO 37151352 42lt10 0]0054 6711 97 001

110 ]605]]2 495 0131014 6711 97 001

112 350013011 53147 007001 6711 97 001

EIIT2 3512J709 6365 OOl003 67t1 97 001

No 3 1215505bull 73197bull 0061003 6121 19 003

11bull _IZImiddot 131middot OOCSmiddot 6121 19 00]

No 17 middot I middot __ middotImiddot 6121 19 003

EIIT2J middotImiddot middotImiddot middot I middot 6121 19 003

111 731J175l7 1151111 001001 12 001

115 bull71W7411bull 751111bull 01CW05 12 001

NUS] 712517t77 1111111 0101001 12 001

11] middot Imiddot __ middot Imiddot 12 001

----Fitlt vaue vivert is baled on log-loe an~u second vbulllue ibull ~on wmiiOO INIYibulllaMd on ttmilot INiytitonly

Bear J 1979 Hydraulics of Groundwater McGraw-Hill Inc New rork New rork

Boulton NS 1963 Analyais of Data from Non-Equilibrium Pumpinq Teate Allowinq for Delayed lield from Storaqe Proceedinqe of the Inatitute of Civil Enqineering Vol 26 pp 469-482

Cooper BB and CE Jacob 1946 A Generalized Graphical Method for Evaluating roraation Conatanta and Su-arizinq Well rield Biltory Alllrican Geophyaical Union Tranaactiona Vol 27 pp 525shy534

Bantuab Ms 1964 Bydraulica of Mella In Advancea inlydroacience Vol 1 Acaclic Preaa Inc New York

Jacob Cl uu Notaa on Detorainin9 Porability by PIIJIPiD9 leotl Onder llator-Tablo Conditione O SGS Open Pile Report

-n IP U75 Analyoio or PIIJIPin9 Toot Dllta rroa Anlootropic OllconUned Aquifou Conoidorift9 Dlllayed Gravity Rooponoo llator aeeourcea bullbullbullbullarch Vol 11 llo 2 pp 329-342

ltallMn RW 1965 Effecta of Water-Table Conditione en WatershyLevel Chan9e1 ar Puapin9 Mella htlr Re1ource1 Reaearch Vol 1 No 2 pp 295-]12

Walton lfC 1914 Practical Upecta of Groundwater Modelinq bull tional Water Nell Uaociation

Walton lfC 1917 Groundwater Puapinq Teata Levia Publhhen Cbllllampr 1Uchi9an

TAILpound2PUMPIING TEST IIESULTS SUMMARY

SUPPLEMENTAL MOM IIIIFSGAOVELAND WEW STE

GROVELAND MASSAOIUSEnS

TIMEmiddotORAWOOWNbull DISTANCEmiddot ORAWOOWNbullbullWEll NO

T(ftl lday) K(ftldbully) s Tft11diy) K(ftdbull yl s

1-SO 37151352 42lt10 0]0054 6711 97 001

110 ]605]]2 495 0131014 6711 97 001

112 350013011 53147 007001 6711 97 001

EIIT2 3512J709 6365 OOl003 67t1 97 001

No 3 1215505bull 73197bull 0061003 6121 19 003

11bull _IZImiddot 131middot OOCSmiddot 6121 19 00]

No 17 middot I middot __ middotImiddot 6121 19 003

EIIT2J middotImiddot middotImiddot middot I middot 6121 19 003

111 731J175l7 1151111 001001 12 001

115 bull71W7411bull 751111bull 01CW05 12 001

NUS] 712517t77 1111111 0101001 12 001

11] middot Imiddot __ middot Imiddot 12 001

----Fitlt vaue vivert is baled on log-loe an~u second vbulllue ibull ~on wmiiOO INIYibulllaMd on ttmilot INiytitonly

Bear J 1979 Hydraulics of Groundwater McGraw-Hill Inc New rork New rork

Boulton NS 1963 Analyais of Data from Non-Equilibrium Pumpinq Teate Allowinq for Delayed lield from Storaqe Proceedinqe of the Inatitute of Civil Enqineering Vol 26 pp 469-482

Cooper BB and CE Jacob 1946 A Generalized Graphical Method for Evaluating roraation Conatanta and Su-arizinq Well rield Biltory Alllrican Geophyaical Union Tranaactiona Vol 27 pp 525shy534

Bantuab Ms 1964 Bydraulica of Mella In Advancea inlydroacience Vol 1 Acaclic Preaa Inc New York

Jacob Cl uu Notaa on Detorainin9 Porability by PIIJIPiD9 leotl Onder llator-Tablo Conditione O SGS Open Pile Report

-n IP U75 Analyoio or PIIJIPin9 Toot Dllta rroa Anlootropic OllconUned Aquifou Conoidorift9 Dlllayed Gravity Rooponoo llator aeeourcea bullbullbullbullarch Vol 11 llo 2 pp 329-342

ltallMn RW 1965 Effecta of Water-Table Conditione en WatershyLevel Chan9e1 ar Puapin9 Mella htlr Re1ource1 Reaearch Vol 1 No 2 pp 295-]12

Walton lfC 1914 Practical Upecta of Groundwater Modelinq bull tional Water Nell Uaociation

Walton lfC 1917 Groundwater Puapinq Teata Levia Publhhen Cbllllampr 1Uchi9an

Bear J 1979 Hydraulics of Groundwater McGraw-Hill Inc New rork New rork

Boulton NS 1963 Analyais of Data from Non-Equilibrium Pumpinq Teate Allowinq for Delayed lield from Storaqe Proceedinqe of the Inatitute of Civil Enqineering Vol 26 pp 469-482

Cooper BB and CE Jacob 1946 A Generalized Graphical Method for Evaluating roraation Conatanta and Su-arizinq Well rield Biltory Alllrican Geophyaical Union Tranaactiona Vol 27 pp 525shy534

Bantuab Ms 1964 Bydraulica of Mella In Advancea inlydroacience Vol 1 Acaclic Preaa Inc New York

Jacob Cl uu Notaa on Detorainin9 Porability by PIIJIPiD9 leotl Onder llator-Tablo Conditione O SGS Open Pile Report

-n IP U75 Analyoio or PIIJIPin9 Toot Dllta rroa Anlootropic OllconUned Aquifou Conoidorift9 Dlllayed Gravity Rooponoo llator aeeourcea bullbullbullbullarch Vol 11 llo 2 pp 329-342

ltallMn RW 1965 Effecta of Water-Table Conditione en WatershyLevel Chan9e1 ar Puapin9 Mella htlr Re1ource1 Reaearch Vol 1 No 2 pp 295-]12

Walton lfC 1914 Practical Upecta of Groundwater Modelinq bull tional Water Nell Uaociation

Walton lfC 1917 Groundwater Puapinq Teata Levia Publhhen Cbllllampr 1Uchi9an

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APPIIIIDIX 8

-ID SOIL 8A11PL1a1 nJR GliAlbull SID AIIALIampIS

NUS CORPORATION AND SU8SIDIARIES

110 ---- - ---- --- _5_~12 - __-~~S-25 fimiddotSD

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1. barcode 558956
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APPIIIIDIX 8

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NUS CORPORATION AND SU8SIDIARIES

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APPIIIIDIX 8

-ID SOIL 8A11PL1a1 nJR GliAlbull SID AIIALIampIS

NUS CORPORATION AND SU8SIDIARIES

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APPIIIIDIX 8

-ID SOIL 8A11PL1a1 nJR GliAlbull SID AIIALIampIS

NUS CORPORATION AND SU8SIDIARIES

110 ---- - ---- --- _5_~12 - __-~~S-25 fimiddotSD

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1. barcode 558956
2. barcodetext SDMS Doc ID 558956

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APPIIIIDIX 8

-ID SOIL 8A11PL1a1 nJR GliAlbull SID AIIALIampIS

NUS CORPORATION AND SU8SIDIARIES

110 ---- - ---- --- _5_~12 - __-~~S-25 fimiddotSD

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1. barcode 558956
2. barcodetext SDMS Doc ID 558956

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APPIIIIDIX 8

-ID SOIL 8A11PL1a1 nJR GliAlbull SID AIIALIampIS

NUS CORPORATION AND SU8SIDIARIES

110 ---- - ---- --- _5_~12 - __-~~S-25 fimiddotSD

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1. barcode 558956
2. barcodetext SDMS Doc ID 558956

APPIIIIDIX 8

-ID SOIL 8A11PL1a1 nJR GliAlbull SID AIIALIampIS

NUS CORPORATION AND SU8SIDIARIES

110 ---- - ---- --- _5_~12 - __-~~S-25 fimiddotSD

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1. barcode 558956
2. barcodetext SDMS Doc ID 558956

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110 ---- - ---- --- _5_~12 - __-~~S-25 fimiddotSD

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1. barcode 558956
2. barcodetext SDMS Doc ID 558956