UNITED STATES DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY I

Geologic Map of the Teller Quadrangle, Western Seward Peninsula, Alarska

By C. L. Sainsbury

Open-file report 19 70

This report is preliminary and has not been edited or reviewed far conformity with Geological Survey standards or nomenclature, GlmmKC HAP OF TRE PBLUR QUADRANGLE, Page WBmSEWAIlD PEHlHSaA, ALASKA Iatduction------1

&ologg------1, &era1 stratigraphy------L P rec-flen roeb------3 IITWIOII The Teller quadrangle the of Kigluaik Group------3 kncluder u%sternmmt tip the lorth to of wdlmer pare------3 American Contsm~aentat its d-at approach Siberia. Ruck snd Paleozoic an: intricately aa Tigaraha Schfat------4 Preenmbrian age interdxad the result in Co1Lier Orth~g~~~------4 of tntenae overthrust faulting the thrust belt [Saimbury, Age---- ...... 4 196%). ~& of the early work on the Sward Peninaulr was by rapid now Group------5 recannaisaance 8nd is now outdated: therefore the geologic data and Upper Pr*drian rocks------5 here baaed upon work mince Age of the upper Precambrian mcka------6 concluaim~presented are principally my Paleomte rocks------a 1958. Except for Smfzb's (1910) work around Worne, the tbwt relatiow were unrecognized mapping; racks------8 during the early raeonnaissmce hence, sock= widely agsu grouped. retaina Cretaceous and Tertiary(?) rocks------8 of dlf ferent were The preseot report Tertiary or Quaternary rocka------9 previous groupings where feasible; where not, older n-8 ara abandoned or wdified Pletstossne roe&------9 . Pleistocene and Holocene upconsolidated depsita----- 9 mmm 9 Gwaral stratigraphy Ore deposit~------.------10 Early workare who mapped par- of the area copsred by thT8 tep6tt Patroleum potential------12 dfstinguirhed md amed several lithologic units. Bmb(in Brooke Reference= cited------U and others, 1901) applled the name tiglualk Serier to the lbesrtwes, achiatu. and granites of the KlgLuaik 14Duntain8, and the nme Kuzitrin Series to pephitie mchisrs and related xockm on the north and south midem of the rormtaha. Ae belted theam rock8 to be of Psleozoie age or alder. iroob rho d the liae Seties, and mtated that it mehted af "lirestmee, graphitic dea and calcareous schlsts with rsnp grteostaae intrusive8 and sow! chhrktic schisba." Re ccmaidered it to be of Hesnzoic md Pdeoroic age: Collier (1902, p. 15) subdivided the 8- Sesies into the Port Clarence Lkstme, of rocks now ansigned to the "elate of the York regloa," a tern first Silurian age, and the Kugryk Gmnp, wtdch consisted of "lnterrtratified used by Knopf (1908, p. 13). limestones, mica scltist~,and graphitic ~ehiat~.~'Hoffit (19131, who "Slate of the York region" .-Tbia infarral mm~is retahd for mapped in the Homz area and in the IEigluatk nDlmtrdns in 1904-5. and ~rapbitic, slaty. or phylritic mdrs of late PrecardBrlm age, rrhich who f-d the agparrnt scratlgraphy LW owph that he defed come originally aswaisted rainly af silt-sired quartz grafua in a latian6 , divided the Kiglualk Group into the Tigaraha Schist and vari- carbonaceous matrix, and hich are widespread over the Sward our intrusive types, and the older crystalline limestunes and gaeiaesr. Fenbsula. Locally, these rock^ id& thin black lirestone. Fbffit (1913, p. 27) also changed the radc of the Hare Series to Plw calcareous graywacke, and, %a the dclrdg of granite, biotite- Group, and stated that it contained principally chloritic schist and andalusire- touwalina rocks. small- gg~lmtsof feldapatbic and elliceow graphitic schist. Fort Clarence tiPestwc.-Tbfa designation is abanhed, for it ~a8 later workers (for exmmple, Sdth, 1910) retained thee DM, and expanded from the original designation to include rocks ranging in addad others to accommodate lithologic variations in restricted areas, age from late Precambrian &rough Mtssissipph. In thh report, arr tbt considersble cdtwiw resulted. 48 pointed wt prepiwsly each Ifmestone amit is ref&& only m the sgsten represen-. (Salnabury, 1965, 1969~), this cwf uaim was caused becauee rocks of Precambrian rocks diverse age and lithologg acre juxtaposed or seedagly interstratified Groug by uidespread thrust faulting that affected the entire Sewad Pminsala Unnamed lower part.--The unnamed lower part of the Kiglueik Group, in the Cretaceous. which ha expoad at the weat base of Phmf'Qmbornjust off the south In the present report, established tsrnfnology is retained where border of the quadraagle, cwtrists of banded quartz-pla@oelaa+ possible, bur, except for the Kigluaik Gtmp, demignafed units are biotite-garnet-paragndno (pegnl), originally calcareow, cut by nlrmer- con~iderablyrestricted. Present urage ir as Follows : ow pis, I--, addikss of madtic gneiss. The ariginal carbonate Kiglaaik Group.-The Klgluaik Group iaclltdea mcks of Pmrianage in am calc-sllicata rock, pith locd bits of coarse-grained calcite. only, comprising all of Maffir' B (1913) units, including the Tigaraha The granitic gneiss dikes are folded mdatt~ated. The gnetssi In the Schist: it includes Precdudan orthogaei~a,but excludee Cretacww lower part of the Kigluaik unit har an exposed thicknescl of 1,500 feet igneous rocks. The Tigaxaha Schtst as here uaed includss soae on mt(IBborn; the base is not erpsed, and the gwiss ia tranaitimal marbles and cnlcareoue sequmcecl, but excludes acme graphitic. into an werlying coarse-grained marble (pw, which here icl about siliceous rocks nm referred to the "slate of the Pork region." 500 feet thick. Husdte and either olivine or montiesllita are chax- Nome Group.-This name is restricted to rocks which are of Precdrian acteri~ticof the marble. Becauee of flowaga and recrystallizatiw, age, and which consist af chladtic achiet d marble scbiat, with the dlevadw fn rbiches's, and meof the original bedding is minor arouats of graphitic, chloritfc scbisr and metammtphosed gab- preeeved. broic rocks. Ma~sivemarble and limestone of Paleozoic and latest The prarble im overlain ebruptly by eddtzional b& gneiss Precambrian age are excluded. ~pSpuJ,which ca1t4.w desilicate mebs d biorlbe s&lst. the Kuzitrin 5etiss.-This mame is abandoned, for it lncluded rockr correl- main difference between the upper end lower aneiemes is that the upper ative with part of the Tigaraha Schist, al well as younger graphitic gneisa ermtaina a larmr awnmt of crrlc-silicate rock and blotitegarnez schist. 3 Tigaraha Schist.-+ithin the area of tae Teller qudrmgle, tbe rocks of this type frm ather areas, I interpret this age as being the Tigaraha Schimt (pa) is eompoasd principally of graphitic biotite time of matemorphism. X believe a Precddan Qe for these rodre i~ chi st, calcaredua biotite schist, end biotite-garnet schist, and it mrrongly suggested but not conclusively proved at thfs time*" abo cmitains several calcar;eolls sequences. 8mraua varfatioas were OD tbe Bamia of these apdates and the abdaat -Logic evidence noted on the south side of the Eigluaik Hwntains, where stamolite that the rocks are much older than the "slate of the York regfm," schist, siliceous graphitic schirt, end calc-silicate rocb occur. which is iteelf older than unfossiliferow rocb below the Lower Or&- MoEfit (1913, p. 21) included graphitic sfliceaus schist that ia wide- deim li*estmes of the York bunteins {Sdosburg. l%5. 1969c>, I spread w the south side of the KtgluaiL lhmtaim with the Tigaraha curtalder the Precmbrian age ast&liehed. Schist, whereas narlier workers considered thin graphitic e&i~tto be #me Group part of the Kunitrin Series (in the present report, these ailiceow, The lome Group (ph), originally named md dacribed by Brooks, graphitic mdrs are referred to the "slate of the Yark regiodr). Bidmrdson, and Collier (1901). but reatnlctd bare to rocka of Within the Tigaraha Schist are eeveral calcareow sequences of Preca&rian age, mists of graenisb schist with mrwa intarcalated considerable thickness. One sequence i~ compicuoua along the north layers of marble and marble schiet, all of which ate intruded by numer front of the Kigluaik Mountains, and was mapped separately as a calcar- om dikes and plugs of altered mfic racks. For the -st part, the eoum eubrmit IpQbm) of the Tigaraha Schlst. A sectLoa measured in the schist (pgcl) fs of magnesian chlorkte, epidote, albfte. headwaters of a small mudet- flowiw iato Windy Cove of Imruk quartz, calcitm, amphibole, and apbeue; locally, garnet and glaucophane Basin from just east of the small body of fine-grained granite cw~imf8 occur, particularly in the east part of the quadrangle. The marble of a lower unit 80 feet thick of marble containing rolled quartz schist (pslaj displays ab&t drag folds overturned to emst or mrth; "rods," a middle uuit 360 feet thick of qwrtrbiotite schist with those overtmnd ea&t mmudly have hodmtd a*as rritlr an intense calcareou~leasmi, pods, and thia bear, and an upper unit 550 feet -at-plane lineation that consiste of cltriatim and almgated new miner- thick of marble. ala. Allnost avarywhere a second plane of foliation cmsscuta the Orthomebe.--The Kigluaik Gmup rock6 are intruded by ummmw earlier mhistoaity. clwrly rewrdiag two o~ta~rphiccycles. All the igneous rocks incltlding a quartrbhtite o~hogneiss(pbgn) vith latble schist layarm cootala a- grdm of q-, which differ=- ous aeeociated coarsegrained pamtites that contain dark tourmaline tiates them from the Paleozoic cabonate rocks. The schi~tof the Iwe and, locally, beryl (Moffit, 1913, p. 26), a8 well am by younger Group $aa not beau found Ln an wquestionable depomitid contact mer granite ad dike rock. the older Kigluaik Group, but it nrruhtre is cnavsrred ta peisa and &+--The Precambrian age of the Kigluaik Group rocb ts baaed cm therefore it probably ir younger than the Kigluaik Group. geologic evidanca and on two age dates, each 750 m.y., by C. E. Badge, Uppar Prmcembrian roch U. S. Geological Surpey (written -. , 1969). who, wing the whole- Bods of this age mumist of the "alate of the Y& region'' (p6s) mdc tubidi-strontium method, dated a merple of the ortbogaeisa and ao rmarlyiag segwmze of iaterbedded, thin-bedded dolodtXc m- (p6gn) from the southeast corner of the Teller quadrangle and atone and argillaceow lirmestone (HI). Included within the "slate of a aqle of the granitic dikes cutting the lawer gneis~on the west the York region" axe diverse lithologic types ouch an graywacke, slate, face of &unt O~born, fuat off the south border of the map area east of carboaaceow miltfee, and thin farboa- IUtw, but ettber the Cobblestone River. Redge stated, "From my experience in dating eiliceoua rlate or carbonaceous siltfte forma the bulk of the unit.

5 Although locally the unit ia intensely defamed, especially war tbrust l'Quadtanglee of 1:250,000 scale in Alaska are divided fato faulte, much of it still dieplay original sllt-sized quartz grain8 and 1:63,36iJ-scale quadrmgles br dimfoa alang latitude and longitude relict depositional feature#, which im in sharp contrast to rocks of Ilnu as fallows: Beginning frm the eautheast comer, each 15 etes the Moue Group, *me original se-rarg faahuss are setda meen. af latitude marks the north hdary of a Une of qead-glem numberad Above the slate, with a contact that in the York Mountains is A. B, C, D; to the rrerit, each 30 -tea of loagitude raw tha met ttanaitid (Saimba~.1965. 1969~1,is a thick sequence of tbiw bolmdup of a line of paadrangles numbered 1, 2, 3. 4. 5, 6, 7. bedded doldtic l-toae dth rhg thpically interbedded argillaceous (p61) -11 veialete. Zlmestaae ahich contains ubtquitowi quartz This may reach nearly 13,000 feet (Seiasbury, 1969~). The Lower Ordovician limestone oaquence is so deformed that ite true thickrase cannor be limastone ia trcmeitional into an werlying thin, black, Eissile shale determined, but it is at least several hundred feet thick. The quartz 50-100 feet thick, which is transitional into overlying dark limeatone veinlets these from lithologically distinguish rocka eimllar Ordovician (OshL) and dolomitic limestone (Oshd) . The time boundary between Early rocks. to Hddle Draovldan occur8 duet belw the black shale. The Mlddle Gabbm (p6g) ma dib, sills, 8nd irregular plutons intrudes the Orddden rocks meed 2.400 feet fn thidraese. OPerlging these are in at me place. elates manp places and the argillaceous l-toaee fassillfemw dark muse aad doldtic lhzstonc of Late Ordwfcian Gabbra and related & are of two ages-the older i8 qletely age which are beet expoaad west of the Doe River, in the Teller B-4 recrystallized, and the younger retains e relict igneous texture. JR quadrangle, although they occur elmhere. Foaaib suggeat that Lower the eaet part of the Teller quadrangle, the alder mafie racks- and the Silurfan rocks are abemt. A diaconfomity at the top of the OrdoVi- enclosing Nome Group rocks locally have bwn ctlaverted to glaucophane- elan is secognizad at many places in the Soviet Union (Boueot, 1969). garnet rocks of tbe blueschiat fades [Sainsfrutg and others. 1970). Beaume die ti- bwlies within tfie qpperw#it dark linestone, ad The do gabbme not intrude the Pataowic rocks. la not tasppeble on litholog, tbe unit includes sae Siluriea m&a. Age of tba upper Precdrian rocks.--The slate adoverlying lf~re- rmd hence La ahwn an SOdl. The dark Ifreatme appara tramitioaal stoaes axe dated a~lPrecddan because the mckg are unfossilifsroua, into overlying Silurian limestone. [Sl), which fa light browmiah gray. more deformed chan the overlying tower Ordovician limestones, contain The Upper Ordovician and Silurian sbckrr together exceed 1,000 feet in quartz veim, and am intruded by numerous gabbroa that do not intrude thickness. Ordovician limestones. the tower The Devontan System ia represmted by dark-celord sparsely foa- Paleomic rocks siliferous limetome and doldtic limestone (Dl) aggregating savaral The oldest Paleosoic rocks cmimr of a very thick sequence of hundred feet in thtckness expo~edin a windm in thrust sheeta of unmetmrphoaed fosailiferous limestone, doldtic limeatone, and tmdifferentiat~dlimeatow of late Pracambrian and Early Ordwician argillaceous Wstrrae (01. Qal) of Eaxly Ordddan age. Where age north of tbe Agiapuk Biver. Dwodan liraslane is exposed also In s-ed in detail in the York IkuntaL~s(Teller 8-4 and G4 quadre the $emd- qaadraugle 1:2M,000 which adjoins the Teller quadrangle I/ gles) ,- these rocks aggregate at least 7,000 feet in tbidcnmss, aud on tbe east. The Hasissippian Syat- is rapresented by intricately deforred and recryaralliaed limestone with subordinate ahale (M)near Cape Mountain at the *resterolDst tfp of the Seorard Peninsula (Collier and Perriarg or Quaternary rocks others, 1908). The rocks of Hississippian age, which form the upper dn ertensive volcmic field south of the Agiapalr Biwer cmtatns plate of the Wales thrust fmalt, were lsoflindly folded duting east- deeply eraswriac- basalt (QTb) that an be eeen to overlie ward thrusting, and shale beds are broke0 Znto isolated and ~~EEOO~~P lm-olldeted gravel ia a ~ingle-sure near tbe western forks of urns Eragreotrr. Ho estiPate of thickness is poesible, for the rocke the Agiapuk Biver. Tbat tbt lava Helds were ance mre extensive is are so tectoaicdly defaired that for the l~stpart they are converted suggested by eroded r-ts of fhand by breccia necks dedfmto to banded marble. They axe, however, spar~elyfo~siliferoue. Collier, relief, indicating extensive destruction of the original surf- of Hess, Smith, and Brooka (1908, p. 81) reported interbedded "dark mica the lava field. ha this arosion may have taka considerable tim, rchia ts or phyllites," aa well as quartzite; however, this "quartzita" some of the volcaaica may be ae old an late Tertiary, although they i~ a banded fine-grained quartz which ha replaced the lfmecltme imnte- most probably are Pleietocene. fragment^ of ~coriaare found in the diately above the Wales thrust fault, and the phyllite is believed to gravel overlying the York terrace of Pamouth(?) age, and hence the be infolded thruat dice8 of the "slate of the York region." basalt ie at least as old as Pamouth(?).

Cretlteeoum rocka Pleistocene racks Exposed rocks of Cretaceous age con~istof intrusive rock^ ranging Cemented conglomerate (Qpc) of Pleistocene age fom ieolated from gneissic granite to diaba~e. Granitic rocks of at leaet two ages patches over the York terrace of Parmouth(?) age, which notches the are known. The older rock# con~istof a thick and coatinuou~sill of south flank of the York Momtains (Teller B-4 quadrangla). The cm- garnet-bearing granite gneiss (Kgn) exposed for miles along the north glomsrate, which represents old deltaic and allwial gravel, has been side of the Kigluaik Mountains, and the younger Eonus stocks and dikes described Ln detail (Sainabury , 1965). biotite Kgf) the Mountains of unfoliated granite (Kg, in Kigluaik and Pleiutocene and Holocene unconsolidated deposits elswhere in the quadrangle. The gneissic granite is assumed to be of Most of the low at- of the quadrangle are cwered by parendally Early Cretaceous age (although it may be older); the stock at Brooka frozen surficial deposits which include (1) sxtennive silt and loees &untain (east headwaters of the Mnt River) was dated by Manrln blanlcate wer the marine platforms of Sang-n age, (2) glacial mraine Lanpbre, U.S. Ge~logicalSurvey (written comun., 1967) , who used the and outwash gravel of Wiscowin age, and (3) upland silt of €blocme K-hr ethod on biotite, ad obtaiud a calculated of 75.~3m.y. age. Boded uplad aream are -rled by frozen eflt end a thick mt Cretaceow and Tertiary(?) rucks of hmdra Mcbeffectively wsk bedrod. The Pleistoeeoe ad Holocene Bumemus dike8 of grate, diabase, rhyolite, rhyolite porphyry, deposite have been described in detail (Safnsbury, 1965, 1967). andesite, and leoprophpre (W,T&a) occur: as wne of these are Structure gneissic, and aa all tytgpes intrude the tbtsheere, thy are cooaid- The geolo&ic structure of the Teller quadrangle ie m*edby ered at leaf as yormg as Late Cretaceous in age, and sa-= ray be as thwt faulting of hro differant ages. Bqiming probably in tke early young as Tertiary. lid-Cretacerms. botb Precdrien and Palwxoic rocks were thrust east- ward, north-trendlq folb were developed and overturned to the east, ad an c-plme Uaeaticm farred. TIE structural &rain f-d in tbia tectonic cycle fa best ahm ewt of the ktrican Biver, where Precdriaa aud Paleozofc TO&B are intimately intermixed. later in altered graphitic schist near the Kigluaik fault. At Zeaet 2,500 tom the Cretaceous, the uimetmmrpbosed rods of the York Hovnratns mowed of tin ham b- produced frm placer deposits, vrstly fmm Buck Creek. from the south into their present position; these rocka dip north, the near Potato Mountain (Wlligan, 1965), and from Caps Creek ((Mullfgan, thrust planes are but gently warped, and structural trends are mainly 19661, which ia producing currently. Placer gold deporits currently ea8t-west. In the latest Cretaceous, iaolated stocka of biotite gran- are mined at the headwaters of the Right Fork of the Bluestone River ite intruded the tbrust sbeets, and several systers af no& faults in the Teller 8-3 quadrangle; other pl-r gold deposits in the sare developed, sme of which cot the granites. In the Yock Hmmtains, the quadrangle were niued formerly (Collier and others, 1908). In the strmgest syster of aamal faulte strikes about 1. 75'-85' B., and Teller C-2 quadrrmgle gold placers of importnnce were dntd on Sunset south blocks are downthsunm. Faulm of thie system were very important Credc, north of Grantley Harbor, and on the triburariee of Budd Creek. in locaMdng ore deposits (Sainabury, 1965, 1969~1, especially here litmy sdpld placers were dried elseuhere. Cinnabar- ac:-ies lamptopbyre dikes in Eadts interaectd porous zones aloug thrust soae placer gold on the Bluestme River and its tributaries, and sorne faults. plattnu~rgroupmetals are known in auriferous gravela on the Bluestone In the east half of the quadrangle, high-angle faulta of probable RLvar. Tertiary age, striking N. 10'-20" E., are espectally couapicaous, Hamy areas of altered bedrock ere sqled during regSooal map- Sae of these faulta may be active yet, for the eastward-etlrlldag phg, and st-sedirent nuneys were rade Locally. Host of the Kigluatk fault, uhich bcuods the entire north front of the Rigluaik impartant data accumulated before 1969 were released in an open-file lbmtaine and which curs glacial depoeits, apparently is offset as report (Safnsburg and others, 19691, including economic data for parts much as several thoueand feet by north-trending faults. of the Bendclebm quadrangle wnriguwa to the Teller quadrangle; hm The Rtsucrure of the Precambrian rocka in the Kigludk Mountdns ever, one newly discovered area of tin-bearing akarn ia outlined on aware aiqle on superficial examination, but structure as revealed &e presemt w. Tbh riaeralid area is iderred ftm numerous in rocks along the great arch forming the axla of the range ia boulders of fmt-riven kdrock that lie along the lofig ridge betweeo extremely complex in detail. The distribution of lithologic unite ie Igloo Creek and ~medcadRiver in the Tellef B-2 quadrangle, and from lost easily mlzplained as a result of eastward thrusting and foldisg sfastend outcrops of tactite cmfaining flmrlte. Spectrographic on north-south lines, fall- by uplift aod warping m east-rrcst wes. malyses of Mcr tactite show highly ammdas mtsof tin, beryl- liua, and bimutb (>l,MWI ppm Sn, 1,000 ppm Be, ad r1.000 pm Bi). ORE WOSITS The widespread tacrite ia clear evidence of a nearby intrusive. rock, Several distinct type8 of lode and placer deposits in the Teller and the abundant fluorite, tin, beryllium, and bismuth are similar to quadrangle are af economic importance, the Lost River tin mine being those in tin-bearing deposite elsmdtertc oa the Sward Peninsula. The the most import- tin hde of the hired States (Knopf, 1908; emtof the daerallzed arsa, which lies on the publle dm,has Sainsburg, 196.4). Lode depasits include tin, tlmgsten, end beryllim not been determined, but the area warrants -re pork. Too, the drala- lodes related to the Upper Cretaceous granites (Knopf, 1908; Sai~burg ages that border the mineraIized area mhould be evaluated for placex and others. 1968; Sainsbusy, 19681, as well as minor lode depositcl of tin end gold. capper localized aloag silicified zoaae above thrwt faults in carbon- ate rocks. Graphite tri economically iqortmr ammts occurs in PmmPOTBATTAl IIE-Q3S CITED With the intense interest in northern Alaskan oil, petroleum Boucot, A. J., 1969, The Soviet Silurian--Recent impressions: Ceol. coqanies are becdng intereltsd in the Seward Peninlula. The extra Soe. America Bull., v. M, no. 6, p. 1155-U62. rtructural complexity of the rocks ie of primary importance in evaluat- Brwks, A. H., asslated by G. B. Richardson and A. J. Collier, 1901, ing the petrolem poteatid of the area. Although mmetawrphosed h reoormalssence of rbe Cspe El- and adjacent gold fields of lhtanes occur in the York lbtmtdas, these limeatonem are part of Se~ardPenhaula. Alaska, in 1900, [Pt. 11 of Recormeissancua in relatively tbia thrust ebeets which overlie srructoraUy coqhrocks. the Cape A- aud FIortm Bay regioas, Alaska, io 1900: V.S. Geol. of Precambrian age, which are mildly to intensely metamcrr Spac. Pub. , g. 1-185. phosad; thus the chancear for oil poole in the mapped area are coneidered Cob, E. H., and Sdmbury, C. L., compilers, 1968, btallic mlneral wry small. lbreowr, although redirpentr of Tertiary age occur offshore resources map of the Teller quadrangle, Alaska: U.S. Geol. Survey ia the Bering and Wcbi Seas (Scholl and Bogkine. 1969), and my opes-file report, 8 p. . map, scale 1:250,000. extend a sbrt distgaee landward of presmt beaches, the caplex: stme Collier, A. J., 1902, A recdssance of the northstem portion of rure in the pre-Tertiary meks also extends seaward beneath the Tertiary Sward Peninsula, -a: U.S. -1. Sumy Prof. Paper 2, 70 p. racks. Petroleum may occur in the Tertiary rocks, but is considered 1904, The tin dqolita of the York region, Maaka: U.S. Geol. ' - -. ... -,- unlikely in the pre-Tertiary rocks as far &--"thrusting goer seaward. Survey Bull. 229, 61 p. Collier, A. J., Bess, F. L., Smith, P. S., and Brooks, A. H., 1908, The gald placere of parts OE the Sward Peninsula, Alaska: U.S. Gwl. Survey Bull. 328, 343 p. Krwpf, &dolph, 1908, Geologg of the Seward Peninsula tin deposits, Alaska: U.S. Geol. Survey Bull. 358, 71 p. EtDffit, F. H., 1913, Geology of the Nome and Grand Central quadranglea, Alaska: U.S. Gsol. Survey Bull. 533, 140 p. hlligan, J. J., 1965, -lade inveatigatiolls. Potato mtaharea, Sward Peninsula. Alselcs: U.S. Bur. Hnes Rept. Inv. 6587. 85 p. 1966, Tin-Lode investigatiura, Cape Btmtaln area. Se~erd Psninarula, Alaska: U.S. Bur. Mines Rept. Inv. 6737, 44 p. Elom, R. J., Jr., 1965, Early Ordovician trilobites from the Seward Peninsula, Alaska: Jour, Paleontology, v. 39, no. 1, p. 17-20. Sahsbury, C. I.. , 1964, Geology of the Loat Biwer rtoe area, Alaska: U.S- -1. So- Bull- ll29. 80 p- 1965, Quatetaarg geology of vestem Seuard Peninmila, Alaska, in Hopkins, D. M., ed., The Bering land bridge: Stanford, Calif., Stanford Ifniv. Prress, p. 121-143. Sainsbury, C. L., 1967, Upper Pleistocene features in the Bering Strait Schnll, D. P., and Bopkcins, D. , 1969, Newly diswv&r& Cenozoic area, Ceologfcal Su-mey research 1967: U-S. -1. SumProf. basina. Befig Sea sbelf, Alaska: hm. ~OC.Petroleum Geologists Paper 575-D. p. D203-D213. Bull., v. 53, ao. 10, p. 2067-2078. 1968, Tin and beryllim deposits of the Central Yo* lhmtaias, Wth, P. S., 1910, Gerrlogy d nineral resourwe of the Solorm ad Geol. western Seward Pwdnsula, Alaaka, Wage. J. 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