Occurrence of Nonpegmatite Beryllium in the United States sei. N C "3A s fl ® [ a GEOLOGICAL SURVEY/ngOFESSIONAL PAPER 318 This report concems work done on behalf of the U.S. Atomic Energy Commission and is pub/Med with the permission of the Gommission F {ZT [ ID ® LinR Am AR \ - UNIVERgHTy or \_ j LIBRARY Occurrence of Nonpegmatite Beryllium in the United States By LAWRENCE A. WARNER, WILLIAM T. HOLSER, VERL R. WILMARTH and EUGENE N. CAMERON GEOLOGICAL SURVEY PROEESSIONAL PAPER 3 1 8 This report concerns work done on behalf of the U. S. Atomic Emergy Commission and £s puNz's/zea’ with the permission of the GCommission UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1959 GEOLOGY UNITED STATES DEPARTMENT OF THE INTERIOR FRED A. SEATON, Secretary GEOLOGICAL SURVEY Thomas B. Nolan, Director The U. S. Geological Survey has cataloged this publication as follows : Warner, Lawrence Allen, 1914 Occurrence of nonpegmatite beryllium in the United States, by Lawrence A. Warner fand others; Washington, U. S. Govt. Print. Off. 1959. viii, 198 p. illus., maps, tables. 30 cm. (U. S. Geological Survey. Professional paper 318) Part of illustrative matter in pocket. "This report concerns work done on behalf of the U. S. Atomic Energy Commission and is published with the permission of the Com- mission." Bibliography : p. 186-195. 1. Beryllium. 1. Title. (Series) [QET5.P9 no. 318] G S 59-196 For sale by the Superintendent of Documents, U. S. Government Printing Office Washington 25, D. C. - Price $2.25 (paper cover) CONTENTS res nok -one bet =s =_» Nature and purpose of report__._____________-.--- Recovery, properties, and uses of beryllium.._.._.. Production of beryllium ore__________________---- Acknowledgments..____.__________________-______-- Field PrEVIOUSWOTK..__..L __. Prescht yeasu-nane~-<«sme Scope of investigationsg..._.._._._______---_----- Ficld Determination of beryllium.....___.______.____.____-~---- Spectrographic analysis...... ir Gravimetric and volumetric analysisg____________--- Colorimetric and fluorimetric analysis _______.____.- Mineralogic methods._._.__________________-------- Boetyl.l.-.:.... Helvite Ofher Radiometric Mineralogy of beryllium.____._._______________-------_-- Crystal chemistry of beryllium minerals._____-__.-.- Beryllium as an essential constituent in minerals.... Beryllium as an accessory constituent in minerals... Sulfides..." Oxides.2~.. ... _ c 20 o on's ame ame a niels is foi a a s Ring and chain Shect -... S... ..-... shes s Framework silicates.............-...---.-..s Beryllium in igneous rOGk$-_______________------------ United States Foreign Distribution of beryllium in igneous rocks_____..... Mode of OCCUTTENCE. .. ___ Beryllium in sedimentary rocks_____________.--------- Clastic Chemical and residual Coal Beryllium in metamorphic rocks_____________.--------- Beryllium in pyrometasomatic and related deposits.... Previous and present investigations...__.....--.-.-.-- Characteristics of beryllium-bearing deposits.... Related Beryllium in vein deposits..____________________----_-- Quartz-tungsten Quartz-gold veing.__._______._____._.__-_..-_-______ Manganese-lead-zine veing.________________------ Other Yeing:l.. -c. ellen ss Beryllium in hot-spring deposits Association of beryllium with other elements._._..___.-.--- Genesis of beryllium deposits._______________.___------ jel F3 EX 6 co 00 00 ~I ~I ~I ~T Co O Or Or Ot h wa wh wh wh bo bo bode Commercial possibilities and suggestions for prospecting.. Description of l0Calities._________________----_----_--- Nevada and California, by E. N. Cameron and L. A. =e Bo aje ma Eiko Star mine, Harrison Pass-_____.___._.---- Good Hope barite mine, Tuscarora Humboldt County Golconda manganese-tungsten deposit. North workings............._... Fouth workings...-............. Occurrence and distribution of ans Lander COUNtY Barite deposits, Battle Mountain area.. California-Nevada Barite Co. Barium Products Corp., Ltd., 'Tom Pinte districb..:....;:......'<..-« Mineral County iL. JIN Rawhide district. -.. -/. -_ ls Nevada Scheelite mine___.__..... Hooper'No. 2 mine:."............ Yankee Girl Desert Scheelite and Gunmetal mines, Pilot _._ Desert Scheelite Gunmetal mine: Manganese-tungsten deposit at Soda- ville.. ...s. SGE mu io os ons Andalusite deposits near Thorne___._._. Green Tale ming... Mine near Green Tale mine__-_.. Nye GabD§ isl {= ~~~ Victory tungsten deposits.____...~ Brucite and magnesite deposits... Pershing County a Rocks in the West Humboldt Range.. Limerick Canyon area__.______._. Panther Canyon area__________.. Rocky Canyon-Wrights Canyon ...le arse en a Results of sampling............. Tungsten area, Mill City district..___. Sutton beds of local usage.... George beds of local usage.... Other rocks sampled_________._._. Rose 'Creck.mine.._............«=-- Rassed Top area_.................% Champion dumortierite mine_.___--.. Page 59 61 63 63 63 63 64 64 64 65 65 65 65 IV Description of localities-Continued Nevada and California-Continued Nevada-Continued White Pine Cherry Creek district.....___:._____. Happy claimgs.............2.:.. Cherry Creek Snake Sacramento Pass Dirty Shirt mine.. "2" :-". "** "" San Pedro mine. _: Minerva ""_" California: _.c __.. BRs LO Inyo CIUNIY . cle ece. rege Nea nee nae e an. oue Tungsten Hills Deep Canyon areg....'..:....... Little Sister mine.__________ Aeroplane (Moonlight) mine. Round Valley Results of sampling......._._._.. Pine Creek district _.~._...._..__.l.__ Pine Creek tungsten mine_______. Tailings from mill of Tungstar MIG: sass. Yaney tungsten prospect, Bishop dis- STICL._. nnn l peee einai ea eel ne aer San Bernardino and Kern Counties._____. cl L0 Union Flatiron-Spanish vein system ___ Arizona, by W.. T: Coohise COURLY - -- -se 2. «aad ens s... Dragoon Mountains....._.L..._...._.._:: Courtland-Gleeson district._________. Gordon mine Abril Little Dragoon Mountains.._____________. Tungsten King mine.............:._ Bluebird Johnson Camp ares».:.......______. Tombstone district.z...._.::. .-.. Mohave County Boriana Ran Francisco district. Pima County _=-.ezclll..... 2092s Worl Empire JLo) _. Helvetiadistrict_ ..-. Pima districts [:D. LLCO Sants Cruz ue Patagonia "_ l_ ___. Yavapai County 000 Boulder Creek New Mexico, .by W. T. Catron an Black Range Colfax County. scads. distriet.._...._.;.___.._}__ Elizabethtown district__.__-_.._.......__. Raton voleanie region................___ likens we ollo Occurrence of beryllium. CONTENTS Page 103 105 105 106 106 107 107 107 109 109 109 110 110 112 Description of localities-Continued New Mexico-Continued Dons Ans __.} Organ Grant County-. sls. Burro Mountains district...___._..._.__. Carpenter Grandview Other _ Central district (including Fierro, Hanover, and Ranta Rita districts).....______.__ Pinos Altos fidalgo Apache No. 2 district..-......___l___.~. Hachita district (including Eureka and Bylvanite Lordsbure ~:~ "bu San -Rimon "__ Lincoln 0102 Capitan "_o Gallinas district Fauna County.. X-"... _ f w:. O- Tres Hermanas Victorio. Geolosy* c L "to - Tungsten and beryllium deposits______ Quartz Pyrometasomatic deposits. ___ ___ Otero _.. _L... _ ® San Miguel County ":}. Roclada .. o- Willow Creek .> Sandoval County- Cochiti Santa Fe l." ull. New Placers district..-..:. Old Placers district: Sierra _._ .la ton} ___ Apache 'No." I district Cuchillo Negro Tron Mountain distriet.___...__..___.____ Socorro {._ cok 00.00 a_ Jones Camp Tacs County...c.:n } _ O0 "f Red River district". _ si Trans-Pecos Region, Texas and New Mexico, by WwW. cl ct . 0 ' G = fntroductioncl.sc:s ccc cite O_o Intrusive igneous bodies and contact zones... Byoenitic l f_} __ Granitic _ 38.0: 00-0 Metamorphic rocks....._...: Wind Mountain ares............-........... Geology ...... ...... sno o. cnl Structure and metamorphism.... ___. Igneous rocks:-.-__...2 .. Occurrence of beryllium...._...;..".___.__ Cave Peak 0... Geology.. ..i l 00 .OO E°, Igncous rodks_............._- _._. Metamorphic Occurrence of beryllium....._...__.___._. Page 113 113 114 114 114 116 116 116 118 118 118 119 120 120 121 121 121 121 121 122 122 122 123 123 125 125 125 125 125 125 125 125 127 128 128 128 129 129 129 129 129 130 130 131 131 131 185 185 135 135 137 138 140 140 140 141 141 Description of localities-Continued Utah, by L. A. Warner and V. R. Wilmarth____--.. Juab and Utah Tintic West Tintie district 8 clill.l..... Topaz Mountain, Thomas Range, by J. C. Olson .s _ sA {ue n l bn cela ue 2p Salt Lake 34-2. Lp. uus... Little Cottonwood district. ._._....-.._... Toocste Colnty ...... ace oce Sheeprock Montana, by L. A. Warner and V. R. Cascade and Judith Basin Counties-___------. Little Belt . Mountaing...-.....-...e......~. Deer Lodge Georgetown district, by W. T. Holser_._._.. Mill Creek Granite County, by W. 'T. Holser-______ ___... Garnet district. Philipsbure Red Lion district.: Jefferson Basin Elkhorn district. Lewis and Clark Marysville district................l..&.. Spring Hill Madison Silver Star Meagher Gordon Butte. Powell County: Pila Ophir district t 10 Priest Page Silver Bow. Butte district. Highland district...._-..3..:........_.. Toll Mountain cus Sweet Grass County =.... /h Haystack Wyoming, by L. A. Warner and V. R. Wilmarth___. .. 0. dal . Tron Rambler mini. .}. .e: 2 1a. sige Strong ay." Carbon Encampment districts zoes. Hanna Rawling afod. _-. 9.0. lc Loe uas Fremont Fort Washakie JL.. Silver Crown district. Natronsg _. Casper Garfield Platte: Halleck Creek area_ ___ Welcome Sweetwater Leucite Superior district.... CONTENTS Page 143 143 143 144 144 145 145 145 145 145 148 148 148 149 149 150 151 151 151 151 152 152 152 152 152 153 153 153 153 153 153 153 153 154 154 154 155 155 155 155 155 155 155 157 157 157 157 157 157 158 158 158 158 158 158 158 158 158 159 159 159 159 Description of localities-Continued Colorado, by L. A. Warner and V. R. Wilmarth__-. Boulder County _________________-_-_--------- Coal cie n.. Chaffee County...... Calumet lll... Geneva claim..s.- _.. __. =. Monarch Mount Antero area, by J. W. Adams____-. Quray .. 0. Sedalia r -W _...__... Winfield district_________________------- Clear Creek County._______________--------- Georgetown district_____________________ Conejos County Platoro-Summitville district_________------ Costillia County .... .s Grayback district. Tin Veta areg.:...l... l_ liad _c sms Custer County. Querida district..._....-......._.._.-.-.- Dolores 4. Rico district. ..._-clc.s. c ail ... Fremont Florence-Canon City area___________ __ --- Garheld Rifle and Bilt Area.. Cunnison County. -.-., Laws Crested Butte Gold Brick Tron Hill aan ce Occurrence of beryllium._-_---__----- Commercial possibilities._._____----- Italian Mountain Snowmass Mountain area___________----- Tincup district. Tomicht Aistrict_ Hinsdale County . sl. Lake City Huerfano:County._. lee Walsenburg area, by W. T. Holser-____-_. Lake ...}. NV Jude Climax mille _. Ju I AIE La Plata County...". ile lL rl _ Purango Las Animas Morley area, by W. T. Holser_._..__.___-. Mifiéral County Creode ...s 22. Wagon Wheel Gap.........-.-...-...=-..- Montezuma =e - Rush Basin.... eo cdm ud Quray Quray district. -. &a Red Mountain Upper Uncompahgre Park County.... =~ sen chee Tarryall Pitkin County.. - cee. -o Baguache County Bonanza district: v Page 159 161 161 161 161 162 162 163 163 163 164 164 164 164 164 164 164 165 165 165 165 165 166 166 166 166 166 166 166 166 166 169 170 170 171 172 172 173 173 173 173 173 173 174 174 174 174 174 174 174 174 174 174 174 175 175 176 176 176 176 176 176 CONTENTS VI Page Description of localities-Continued Description of localities-Continued Colorado-Continued Central United States-Continued San Juan County-. 2.= . . . 176 Arkansas-Continued Eureka-Animas Forks district. 176 Little Rock Mineral Point and Poughkeepsie Gulch dis- Bryant and Bauxite areas, by W. T. Holser. ;n stil - «oal. 177 Tri-State lead-zine district. Silverton -n - 177 Eastern United States, by W. T. Holser-_________. San Miguel County ce 178 Banford, York County, Maine oo.. 2.&L.1_:2__ Ophin digtrigh . = ams Seow . 178 Carroll County, New __. Summit County. -... 178 fron: Mountain. ..s.__-_ Breckenridge district. 178 Red o: n." Montezuma 178 Upper Blue:-River 178 SussziegrzzfijgieNai; I r ger set meres Teller County...... 179 Franiéiin Sl 10} 2. Los _ Cripple Creek district. --- o. 179 § Bry f & Central United States, by L. A. Warner and V. R. Ins? 'Creek district, Rockbridge County, Vir- Wilmarth. .... ... . co ce megan alig pe. 179 Perrot n - Arkansas c als _c el n ole ool lve aul. Lexie. l. u 179 It Beleoted references. . . .c 22 onc cl rena wenn s . be tise cels. Maghet .-.... - 170 NL dub.usuke . Prats ILLUSTRATIONS [Plates are in pocket] . Intrusive igneous rocks of part of the Trans-Pecos Region, Tex. and N. Mex. - Geologic map and section of western area, Wind Mountain, Otero County, N. Mex. . Geologic map of southern area, Wind Mountain, Otero County, N. Mex. . Geologic map of eastern area, Wind Mountain, Otero County, N. Mex. . Geologic map of Cave Peak, Culberson County, Tex. . Production, imports, and consumption of beryl in the United States, and total world production-____________. - Andex map. of localities .listedamiable16.-... __. _._ rear.: _-_ nce tut C02 C a pata d oon n 2. . Schematic diagram showing occurrence and distribution of principal beryllium-bearing minerals.. . Index map showing localities:sampled in Nevada and hs Geologic map of part of the Rawhide district, Mineral County, Nev.... tenons dub u' __ . Geologic map of part of the Desert Scheelite mine, Mineral County,;.Nev. -.. JLYE.22. GX Geologic map of part of Limerick Canyon, West Humboldt Range, Pershing County, Geologic map of a part of Panther Canyon area, Rye Patch, ~.: {ona dastanl. 3st . Sketch of part of north wall, South fork of Panther Canyon, Pershing Cotnty, Neve: cucu? 4 col. cal . « Geologic map of part of Rocky Canyon and vicinity, West Humboldt Range, Pershing County, « Geologic map of vicinity of Oreana tungsten mine, PersHing:-County, -__ Uro il . Geologic map of part of Tungsten area near Mill City,ePershing County, Nev.... -. _2-c_ ginal: c. . Geologic map of the Rose Creek mine and vicinity, Pershing County, Nev.... .... _c. c- .. 2. . Geologic map of the Rose Creek mine workings, Pershing County, _ oo: . Geologic map of tactite body near Ragged Top mine, County, . Sketch cross section of glory hole, Little Sister mine, Tungsten Hills, Calif., showing rock units sampled.... __ - Geologic map showing glory hole level and inclined shaft level of the Round Valley mine, Inyo County, Calif. _ . Geologic map of the lower eastern adit, Round Valley mine, Tungsten Hills, Inyo County, . Geologie map of the Round Valley mine, Inyo County, Ct icant.. - Geologie map of-part of Pine Creek mine area; Inyo. County, Calif.:. ga.. { dada" Fh duean ars. __ ssindex map.of localific¢sampled in 'Arizonae...._..._} fi -:... lust _o lo eat, . Index map of beryllium occurrences in Dragoon Mountains, Cochise County, Ariz. cabin shunt heavies - 32 _ . Map showing localities sampled in the Little Dragoon Mountains, Cochise County, Arig.____.::cs-0 _ G@gology, of the Tunesten' King claims; Cochise County. "Afla._.__. __ __! ~ "min anne anegely. -. 2. s _ Miincs of the San Francisco district Mohave County, ATIZ-._:..__.-...._.. a :o Sail ..... . . Geologic map of part of the Helvetia district, Pima County, Anis-....~. ..... L. _ . Index map to locations of samples from the Pima district, Pima County, Arizg-.-: ___ - Ceologic-map of Boulder Creek area, Y¥avapat County, c. ._ - Index map showing localities sampled in New sole anl . Sketch map of localities sampled in the Cimarroncito district, Colfax County, N. th: al..... . Map of post-Cretaceous volcanic rocks of the Raton region, New Page 181 181 181 181 182 182 182 183 183 183 183 185 186 197 41 58 62 69 72 T3 73 74 T5 T8 T9 80 82 88 89 90 92 94 95 99 100 102 104 105 106 108 109 111 Ficur® 32 33. 34. 35. 36. 37. 38. 39. 40. 41. 42. 43. 44. 45. 46. 47. 48. 49. 50. 51. 52. 58. 54. 55. 56. 57. 58. 59. 60. Tasos ~ o g at g pog go 1 p b} ho ho ho ho h hD bJ st det ged fot feds fest Go ~I O Gu Q N - © 4 Q0 ~T O Oum GJ N i O CONTENTS . Map of volcanic rocks of southeastern Colfax County, N. Mex.. 2,110 m com wena a nus ole ri aie a blaine Geologic map of part of the Carpenter district, Grant County, N. Index map showing localities sampled in the Apache No. 2 district, Hidalgo County, N. _- Tungsten and beryllium deposits in the Victorio district, Luna County, N. Geologic map of the New Placers and part of the Old Placers districts, Santa Fe County, N. Mex-_________._- Index map of the Apache mining district, Sierra County, N. Mex_..:o Geologic map of Wind Mountain, Otero County, N. Index map of Utah, showing localities a an abbe eon st B Geologic index map showing locations of areas investigated in Sheeprock Mountains, Utah________________- -- Geologic sketch map showing occurrence of beryl in Hard-to-Beat Canyon, Sheeprock Mountains, Utah-_--_-- Geologic sketch map of northwest contact of granite stock, Sheeprock Mountains, Utah-___-_____________--- Index map of Montana, showing localities sampled.__L. .-.. 2s cle ane celts ie @ - Ge Sketches showing geology in road cut on U. S. Highway 89, in T. 12 N., R. 8 E., about 10 miles south of Neihart, Mont.. 2... ... .. il ene al 22 a dure Suid a 2 aik a a. ale nin mie aie min bm al ied n rape a in ie eela man trie orie ele a e si erent ale ie eine i= te »In ae b Index and sketch maps of contact zone near Mount Haggin, Anaconda Range, Deer Lodge County, Mont.... Index map of Wyoming, showing localities em -se 4B Geologic map of Iron Mountain magnetite deposit, Albany County, Geologic sketch map of part of Halleck Creek area, Platte County, Index map of Colorado, showing localities sampled __... --it cdank cles bie ou - sll mane En Geologic map of Calumet mine, Chaffee County, Colo.... - .._ .- - - sew emel o sc lh erences ial he an one cials a - 4 Geologic sketch map of area near head of Taylor Gulch, Chaffee County, Geologic sketch map of vicinity of Star of the West workings, Grayback district, Costilla County, Colo..__-_.. Geologic map of Iron Hill area, Gunnison County,,Colo s ad cason a ank - a on - o C en - mial hew boe mike io nailed m a a Geologic sketch maps of parts of Italian Mountain area, Gunnison County, Colo Geologic sketch map of tactite zone near head of Yule Creek, Snowmass Mountain area, Gunnison County, Colo.. Geologic sketch map of part of northern Tomichi district, Gunnison County, Index map showing localities sampled in the Central United Geologic map of Magnet Cove, Ark., showing localities: sampled. __ ._ cou cuss si cenn enlace acta a ole Geologic sketch map of area in vicinity of Cove Creek bridge, Magnet Cove, Index map showing nonpegmatite beryllium occurrences investigated in the Eastern United States-_________-- TABLES . Comparison of quinalizarin, quinizarin, and morin methods for determination of beryllium in rocks and minerals Minerals in which beryllium is an essential constifuient_-L. L _- 01.01 unl oem L eus ble m w t a blo filed HO de I a 'ad . Minerals in which beryllium may be an Garnet analyzed for beryllif®., .. _. ...... . oun n conn e a a mina mie an aim n alel in' al alie i mals hl io a hl oe an be tM n ole in tale ia it CE tila in he a+ a hoa Ne - athe Analyses of idoecrase for ~~ - - -. . _. - => ~ -=- -- eme ale bn mus mons iod milia hie ol lols he n ab ane i I hem ia ie oo Ie ddd Afr did ee h obie . Beryllia content of 14 samples of cuase .less ce cane cenas aln dues k ad ue . Beryllia content of igneous rocks of the United States, as Beryllia content of igneous rocks of the United States, as analyzed for this study . Beryllia content of igneous rocks from foreign . Beryllia content of sedimentary rocks other than coal in the United . Beryllia in ash of coals of the United lieu os loud alek tua s stole aH Lies ue o mem . Beryllia in pyrometasomatic rocks from Germany, Norway, and . Beryllia content of some pyrometasomatic and related deposits of the United States-._..______________------- . Beryllia in some veins and related deposits in the United States.-__. LL soot uel a - a . Spectrographic analyses for other elements in samples analyzed for beryllium . Other spectrographic analyses from the files of the U. S. Geological . Beryllia in samples from Harrison Pass arega.uL. ...... l=. o c ign Wik a ale mid be ee's he . Beryllia in samples from north workings, Golconda manganese-tungsten depositL_________________________--- . Beryllia in samples from south workings, Golconda manganese-tungsten deposit-_________________________--- . Beryllia in samples from the California-Nevada Barite Co. . Beryllia in mill products from the Tem Plute . s+ . Beryllia in samples from the Nevada Scheelite mine. . Beryllia in samples from the Hooper No. 2 mines-___z_L....___ _ ton . Beryllia in samples from the Yankee Girl seas . Beryllia in samples from the Desert Scheelite mine. s. os . Beryllis in samples from the Oreen Tale -t ances . Beryllia in samples from inner contact zone, Panther Canyon . Beryllia in samples from outer contact zone, Panther Canyon VHI Page 112 115 119 124 126 128 136 144 146 147 148 149 150 150 156 157 158 160 161 162 165 167 170 171 172 179 180 181 182 VIII CONTENTS Page TABLE: 20. ~Beryllia in samples from the Rocky Canyon- Wrights Canyon area- T4 80; Beryllis in samples from the Sutton beds of local L. LEL 76 31. ~Beryllisa in samples from the George beds of local usage. _- __ TT 52. Beryllia-in samples from Humboldt Hilt and Stank Hill NL 78 83. Beryllia in samples from the Rose Creek lil _ {re fol 81 84. Beryllia-in samples from the ragged Top _ col Ch tMmaupl oi 81 5b. Boryllia in samples from the Champion mine. {EHO LOBO OU prep 83 86.-Boryllia in samples from the Happy claims.. MI LOA 83 87. Beryllis in~samples from the Dirty Shirt cousin ObOt DLO Cop L lub 12] 85 88. Beryllia in samples from the. Minerva distriet..=cl:.c LLL fn oar c 85 69. Beryllisa in samples from the Little Sister mine Do Liu [raed {ass 87 40. Beryllia in samples from the Aeroplane ages 0 UL up OLL 8T 41. Beryllia in' sautples from the Round Valley mine.. 91 42. Boryllia tou samples from the Pine :Créek .._ tse 92 49. Boryllia in samples from the Yancy prospect ... 81. tD OC LOP ". 92 A4. Beryllia in samples from the Union mine.. s-... } {saz cl OO L rufen cl mam seul cul 93 45. Beryllia and tungsten in samples from the Little Dragoon 97 40. Beryllia in mill tailings from the San Francisco LLCO. _ 103 47; Beryllia in samples from the Helvetia LCC _ ___ 103 48. Beryllia in samples from the Pima tatt oal l { ou 105 49, 'Boeryllia in samples from the Elizabethtown district.. co {aco ofl 110 50. Correlation of volcanic rocks and related units in the RAbON FEeGIONL 110 51. Beryllium and other elements in volcanic rocks of the RAtON 113 52. Average mineralogical composition of volcanic rocks of the R&ton regION___________________________________ 113 58: 'Bery Hain samples from the Organ district LOLOL l:uue 114 54. - Beryllia in samples from the Carpenter districts.. st __ IOI 116 565.) Beryllia in samples from the Central district:... Prous Mon 117 56. Beryllia and tungsten in samples from the Victorio district . 122 57. Beryllia in samples from the New Placers district.... .l... ".. M else M Bl 127 68. Beryllta in samples from the Red River district. :L .if c" ooc is consul. ci pith 130 59. Beryllia in intrusive rocks and contact zones of part of the Trans-Pecos 132 60. Anvfalysesiof HIfFCONINIIM - 22 - nre ae 2 anl ce anno o nae nnn na nanan an onan e nene n ane anne ana ea a anl neat d 138 61. Beryllia in samples from Wind g r ann 139 62, Analyses of hornfels from Cave e 141 63. Beryllia in samples from 142 64. Beryllia in samples of granite and aplite from Hard-to-Beat 147 65. Beryllia in minerals from contact zone, Mill Creek area, (#161 66:-Boryllia in samples from mine dumps at Butte, LG. OO EL LLL -_ 154 67. Beryllia in samples from Washoe Reduction Works, Anaconda, 154 68. Boeryllia in samples from Halleck.Creck ATOR» . .s... ane etn malin buna aas ow. 159 60. Beryllia in samples from Iron Hill, -OOIO. - ... -. .-.. = ls. un wen ne an ae aie one calne n. ale awk b bald a e aol ban k sigh 169 70.- Distribution -of beryllia in rock types at Iron Hill, Colo-...._-.._c:scc0lllsl selec reds cld ogi 22s 169 TA. Beryllia in samples from the. Tineup distriet.. _..__zcl__u.sllL. _. L L..: sl s. ~ fg Ta. Boryllis in samples from the Lake City LOL OED QOL AL 173 79. Beryllia.in samples of -mill products from Climax, L tot 174 74. Beryllia in«amples from the Rod Mogantain'districts_c__: 0.0L. __O__- _ Li ck foud oublier dl O 175 T5 Beryllia in samples from the Tarryall district.... dos dogebe tout iL _J] 176 76. Beryllia in samples from the Eurcka-Animas Forks district.. 177 77, Beryllia-in samples from the Golden Oyole _ pault. ono id vill. ued 179 78, Beryllis in samples from Magnet Cove, oo ious ie oor ain Butte 180 79. Beryllis and in samples from Tron Mountain,: NSH Caso soup ae eo ui pe oul 183 80. - Beryllium in samples from the Becmerville area, New Jersey {_L O DOO L IS 188 S1. Boryllfa in mill:-products from the Franklin 000.000 00. ils O 184 82. in minerale from the Franklin district. cc Cita 185 THE OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES By A. Warner, Wiurram T. HonsER, VrEru R. WILMARTH, and Evern® N. Camrrox ABSTRACT The demand for beryllium in industry increased rapidly dur- ing and after World War II, establishing a trend that is likely to continue. Production of beryl from pegmatites, the only present source of beryllium, has lagged far behind annual con- sumption in the United States, and even with heavy imports, an adequate domestic supply has not been assured. This con- dition has directed attention to nonpegmatite deposits. During the period 1948-50 the U. S. Geological Survey conducted a pro- gram of field, laboratory, and library research to determine the occurrence and distribution of beryllium in nonpegmatite rocks and mineral deposits, and to appraise the extent to which these might furnish beryllium ore. Although no deposits of present commercial value were found, the investigation has set criteria that will be of value in future prospecting. The average beryllia content of the lithosphere is about 0.001 percent. Beryllium is thus more abundant than certain other metals, such as arsenic, gold, silver, tungsten, and molybdenum. Unlike these elements, however, beryllium does not readily form sulfides and oxygen salts, which constitute the bulk of metal- liferous ores. Because of its small ionic radius, resulting low coordination number, and strongly electro-positive character, crystal structures that will permit high concentrations of beryl- lium in minerals are comparatively rare. It forms only a few stable minerals of its own, such as beryl, helvite, chrysoberyl, and phenakite. In other silicates, including the common rock minerals, it may replace elements such as silicon and aluminum to a slight extent. Under special conditions, as when it fills normally empty lattice positions in idocrase, it may be present in appreciable quantity. As an accessory constituent in rock minerals, beryllium is somewhat more common in granitic and feldspathoidal rocks than in other igneous rocks. Its principal occurrence is in beryl in granitic pegmatites. Other than in pegmatites, beryllium minerals are found chiefly in quartz-tungsten veins and pyro- metasomatic deposits. Small amounts also occur in other types of veins, particularly quartz-gold and manganese veins. In most of these occurrences beryllium is found with fluorite; in pyro- metasomatic deposits it sometimes occurs with fluorine-rich befyllian idocrase. Many sedimentary rocks contain small quantities of beryl- lium, particularly those formed by residual concentration, as the metal hydrolyzes in a manner similar to aluminum. For the most part, however, beryllium tends to be dissipated by processes of weathering and sedimentation. Under simple meta- morphic conditions, beryllium is not easily mobilized, and there- fore it is not concentrated in metamorphic rocks other than pyrometasomatic deposits. Pyrometasomatic deposits and feldspathoidal rocks were sam- pled at many localities in the United States. Only a small pro- 467945-59--2 portion of the pyrometasomatic deposits contained detectable quantities of beryllium; the richest are the deposits at Iron Mountain, N. Mex. In the feldspathoidal rocks beryllium was found only as an accessory constituent in rock minerals. Some of the vein deposits investigated have promise as pos- sible sources, but sampling was not sufficiently detailed to fur- nish a basis for calculating reserves. In places the beryllium content compares favorably with that of beryl pegmatites. Min- ing of these deposits will depend on an increase in price of beryllium, improved beneficiation methods, and utilization of coproducts and byproducts. INTRODUCTION NATURE AND PURPOSE OF REPORT Technological developments during the past decade have greatly increased the demand for many minor metals. Beryllium, because of its peculiar properties, has come to assume great strategic importance. Spe- cial alloys containing beryllium are in wide demand in modern industry and their use is restricted chiefly by the short supply and relatively high cost of beryllium metal. Beryl-bearing pegmatites, so far as known in mid- 1956, constitute the only commercial source of beryllium. Because high-grade domestic reserves are small, the United States has been forced to import most of the beryl it uses. Recently attention has been focused on rocks other than pegmatite as potential sources of beryllium. During the past century many beryllium- bearing minerals have been reported from a variety of rocks and mineral deposits. Only a few of these min- erals are common and many are exceedingly rare. However, beryllium is evidently much more widely dis- tributed in the rocks of the earth than had been as- sumed previously, a discovery that suggests the possi- bility of locating new sources of supply. A program of field, laboratory, and library research to formulate workable criteria that might be used in the search for beryllium ore in nonpegmatite rocks was begun in 1948 by the U. S. Geological Survey on be- half of the Division of Raw Materials of the U. S. Atomic Energy Commission. It had as its objectives (1) to obtain information on the distribution, grade, 1 2 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES and size of domestic deposits of beryllium in nonpeg- matite rocks, (2) to determine the types of rocks and mineral deposits most likely to contain beryllium, and (3) to suggest favorable areas for prospecting. The results of these investigations are set forth in this report. During the early stages of the fieldwork, all types of rocks and mineral deposits were regarded as poten- tial sources of beryllium, and materials of wide vari- ety were sampled and tested spectrographically. Spe- cial attention was given to those types that were thought to be most promising on the basis of earlier investigations. Much of the material regarded as beryllium bearing in this report is too low in grade to be commercial by present standards. However, the consistent presence of beryllium in certain types of de- posits, even though in very small amounts, seems to mark these for further study, and its consistent absence in certain other types of material seems to exclude these. RECOVERY, PROPERTIES, AND USES OF BERYLLIUM Beryllium was discovered in 1798 in beryl by L. N. Vanquelin, and in 1828 Wohler and Bussey succeeded in isolating the metal (Parsons, 1909, p. 77). Proc- esses for the preparation of beryllium, except on a lab- oratory scale, were not developed until late in the 1920's. Since then the price of the metal has decreased from $200 to an average of less than $100 per pound. Beryllium metal is produced by the Beryllium Corpo- ration of America at Reading, Pa., the Brush Beryl- lium Company of Cleveland, Ohio, and the Clifton Products Company of Painesville, Ohio. Details of beryllium metallurgy are given by Kroll (1945) and Kawecki (1946). Beryllium is a metallic element belonging to the alka- line-earth family, which constitutes group 2 of the peri- odic table of Mendeleeff. It has many properties in common with other members of this group, which in- cludes magnesium, calcium, strontium, barium, and radium. It also closely resembles aluminum in chemi- cal behavior. Pure beryllium is rather brittle but can be hammered, forged, rolled, and polished. It may be alloyed with many other elements, of which copper and aluminum are the two most commonly used. Its hardness, depend- ing on the amount of impurities, ranges from 6 to 7 on the Mohs scale. It is one of the lightest metals, the specific gravity being 1.85, as compared to 1.75 for mag- nesium and 2.7 for aluminum. Other valuable prop- erties of the metal are a high modulus of elasticity, a low electrical conductivity as compared with common metals, and a high resistance to heat and corrosion. Beryllium has the lowest atomic weight of any element that is crystalline at normal temperatures and, there- fore, absorbs few X-rays; this makes it useful as win- dows on X-ray tubes. Because beryllium also has a low absorption cross section for neutrons, it is comparable to deuterium and graphite as a moderator and reflector in atomic piles (Smyth, 1945, p. 62). Besides slowing neutrons without absorbing them, beryllium produces neutrons more easily than any other element, when excited with gamma or other radia- tion (Russell and others, 1948). The reaction is as follows: Be'{+y>1.65 mey --- Bef-+n; B € 10-13 see e ---> _- 2 He". It is used as a neutron source in laboratories and in neu- tron logging of wells. Beryllium imparts to its alloys lightness, hardness, strength, and resistance to heat and corrosion. When alloyed with aluminum, magnesium, and zinc, it forms a protective coating of beryllium oxide on the surface of the metal. Beryllium-aluminum alloys have promise in high strength-high temperature applications where lightness is important (Raynor, 1946). Beryllium-cop- per, one of the most useful alloys of beryllium (Yar- ham, 1945; Williams, 1946), combines high electrical conductivity with high strength and is used extensively in current-carrying springs, in telephone equipment, and in pressure gages, as well as in bushings, cams, and sleeves. A beryllium-copper alloy with nonsparking qualities is used in the explosive and petroleum indus- tries where dangerous dust or vapor conditions exist. A beryllium-copper-cobalt alloy that combines high elec- trical conductivity with heat resistance has recently become important in the manufacture of electrical equipment. Because beryllium oxide melts at 2,5¥0°C and is re- sistant to corrosion, it has been used to some extent in crucibles and electric furnace parts. Beryllium nitrate added to thorium nitrate solution is used in the manu- facture of gas mantles, to strengthen the oxide skeleton. Beryllium stearate is used in printing inks, beryllium nitride in making C*, and other beryllium salts are used in pharmaceutical preparations. If beryl is sub- stituted for feldspar in the manufacture of porcelain, the product has high electrical resistance and low ther- mal expansion, properties that are necessary in airplane spark plugs. Emerald and aquamarine, transparent va- rieties of beryl, are highly valued as gem stones. PRODUCTION OF BERYLLIUM ORE In mid-1956 the only known commercial source of beryllium is beryl, mined from granite pegmatites and INTRODUCTION 3 recovered by hand sorting. -In 1951 the world produc- tion of beryl concentrates totaled about 50,000 tons. Nearly all of this amount was produced between 1980 and 1951 and more than two-thirds from 1940 to 1951. Foreign production is chiefly in Brazil and Argentina, though India and Australia have at times contributed substantial amounts. In the United States, the Black Hills region of South Dakota is the main producing area. Beryl has been mined also in New England, Colo- rado, Virginia, North Carolina, Arizona, and New Mexico. The status of the United States with respect to beryl supply is summarized diagrammatically in figure 1. Domestic production and imports of beryl in relation to world supply are shown for the period 1986-51. The dependence of the United States upon foreign sources is clearly indicated. Since 1940 the United States has produced and imported, on the average, somewhat more beryl than it has consumed, but current trends indicate that this surplus may be reduced in the future unless domestic production is increased. Known reserves of coarse beryl ore are small, and any marked increase in supply must come from deposits of a milling type. The U. S. Bureau of Mines has experi- mented with methods of beneficiating low-grade beryl ore and results are encouraging (Lamb, 1947; Sneddon and Gibbs, 1947; Kennedy and O'Meara, 1948). Fatty- acid reagents are used in a flotation process to separate beryl from other minerals. High recovery has been obtained from ores containing more than 0.35 percent BeQO, and fair recovery from ores containing less than that amount, some as little as 0.08 percent. Helvite re- sponds to similar treatment. Feldspar, mica, and other minerals may be recovered as coproducts. Quantitative spectrographic analyses for beryllium were made under contract to the U. S. Geological Sur- 7000 -] 6000 - +A 4000 - & .\ w / +, .'/ Z x / 8 / \: / ~U, S. \ = s \ U. S. imports f p § = 1 el t id ring A) i> C: o 3 < \| 1 I 2000 - I, 1 1 : l, / ‘\ 11 1000-7 "TN V 5000-| / World production / e U.S. production HE erm. 13 _,Z/‘/'—.—'\_ ./ - & pt 4 2k -t --a 22> o |- I 1 T I I I I I I I I T 1936 1939 1940 - 1941 1942 1943 1944 1945 1946 1947 - 1948) 1949 1950 1951 T 1938 FIGURE 1.1-Production, imports, and consumption of beryl in the United States, and total world production. T 1937 4 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES vey by the Saratoga Laboratories, Inc., and the Strock Laboratories, Inc., of Saratoga Springs, N. Y., and by the National Spectrographic Laboratories of Cleveland, Ohio; check samples were also analyzed by the Geo- logical Survey. All semiquantitative spectrographic and chemical analyses were made in the laboratories of the Geological Survey. ACKNOWLEDGMENTS Without exception we found owners and operators of mining properties cooperative in making available samples and geological information. The officials of the American Smelting and Refining Co., Tucson, Ariz., the Coronado Copper and Zinc Co., Johnson, Ariz., and the New Jersey Zine Co., Franklin, N. J., made available some of their own analyses for beryl- lium and other elements, L. H. Bauer of the New Jersey Zinc Company, James Gilluly of the U. S. Geological Survey, D. M. Henderson of the University of Illinois, F. A. Hildebrand of the University of Chicago, V. C. Kelley of the University of New Mexico, R. G. Knickerbocker of the U. S. Bureau of Mines, E. S. Larsen, Jr., of Harvard University, M. D. Lyons of Beryl Ores Co., J. H. C. Martens of the New Jersey Bureau of Mineral Research, and officials of Climax Molybdenum Co., the Anaconda Copper Mining Co., and the Utah Copper Co. generously supplied samples and specimens from localities that we were unable to visit in the field. Messrs. D. M. Henderson, C. T. Gris- wold of Albuquerque, N. Mex., and D. S. Tedford of Columbus, N. Mex., were particularly helpful in sup- . plying unpublished results of their geologic mapping. We are grateful to the University of Colorado, Cor- nell University, the University of Wisconsin, and the New Mexico Bureau of Mines and Mineral Resources for the facilities lent us. FIELD INVESTIGATIONS PREVIOUS WORK Most information about the occurrence of beryllium in rocks has come from geochemical studies of trace ele- ments. The pioneer work on the geochemistry of beryl- lium was that of Goldschmidt and Peters (1932), who concluded from their spectrographic studies of many rocks that the beryllium content of granites and sye- nites tends to be noticeably greater than that of olivine- bearing and other mafic rocks, and that beryllium is found commonly in the contact metamorphic products of calcium-rich sedimentary rocks, notably in such minerals as idocrase and axinite. They noted the ap- parent similarity of beryllium to aluminum in the proc- esses of weathering and sedimentation, and their later studies indicated the presence of small amounts of beryllium in English and German coals (1933). Earlier, Washington (1931) had pointed out the possibility that beryllium had been overlooked in many chemical analyses of rocks, particularly nepheline syenites. Other studies were made by Tolmacey and Filippoy (1934), Zilbermintz and Rusanovy (1936), Szelenyi (1937) , Oftedal (1939), Sahama (19452), and Rankama (1946). In the United States Sandell and Goldich (1943) studied the minor elements in igneous rocks, including the beryllium content of nine samples of granitic rocks. During World War II the U. S. Geological Survey collected a large number of samples from mines and mills throughout the country, most of which were analyzed spectrographically for beryllium and other rare elements (Kaiser and others, 1954). References to the occurrence of beryllium-bearing minerals are numerous in geological literature. Beryl and phenakite have been reported from quartz veins at many localities throughout the world, and helvite has been noted in several manganiferous veins and in con- tact metamorphic deposits. Some idocrase and allanite have been found to contain beryllium, and minor amounts have been reported in garnets, micas, and many other minerals. Before the present work, the only nonpegmatite beryllium deposits in the United States that had been studied in detail were those at Iron Mountain, N. Mex. (Jahns, 1944a, 1944b; Glass and others, 1944), where minerals of the helvite group occur rather abundantly in unusual tactite deposits. Information concerning the occurrence of beryllium was summarized by Fleischer and Cameron (1946), who suggested that in addition to pegmatites, potential sources of beryllium include contact-metamorphic zones, alkalic intrusive rocks, coals, and bauxite de- posits. PRESENT WORK SCOPE OF INVESTIGATIONS With the aid of clues to the occurrence of beryllium suggested by earlier investigations, a field program was planned which would enable investigation of as many favorable areas as possible. Time did not permit sampling of all the localities that were considered, but those sampled are sufficiently numerous and widespread to be considered representative. Fieldwork was done during August-November 1948 and June-September 1949. A total of 23 man-months was spent in actual field work in connection with this program. In August 1948, alkalic intrusive rocks of Tertiary age in western Texas and southern New Mexico were investigated by Holser and Wilmarth, During Sep- tember, October, and November, 1948, fieldwork was DETERMINATION OF BERYLLIUM 5 continued in Colorado, Wyoming, Arkansas, and the Tri-State lead-zinc region by Warner and Wilmarth. In the winter of 1948-49 samples collected in 1948 were analyzed for beryllium and studied mineralogically. The results were used to plan fieldwork for 1949. The program was expanded in 1949 in order to in- vestigate areas in Nevada, California, Utah, Montana, and Arizona, as well as to continue activities in areas previously studied, and three parties consisting of two men each were actively engaged in fieldwork. Holser and W. I. Finch returned to western Texas for de- tailed mapping of two alkalic intrusive bodies, and investigated many localities in Arizona and New Mex- ico, spending 2 months in the field. Work in Colo- rado and Wyoming was carried on during July and August by Wilmarth and P. L. Cloke. Cameron and J. H. Macleod spent 6 weeks investigating a number of mining districts in Nevada, California, and Utah. The fieldwork was concluded by Warner and Wilmarth who investigated several mining districts in central Montana and near Salt Lake City, Utah, in Septem- ber 1949. Several localities in New England were visited by Holser in May 1950. During the winter of 1949-50 analytical and mineralogical work was con- tinued, and compilation of results begun. FIELD METHODS In planning the field program, a choice had to be made between sampling a few localities in great detail or a larger number of areas somewhat superficially; the latter alternative was chosen. This imposed many difficulties in obtaining representative samples. Some of the deposits selected for sampling are large and ex- tremely variable. Literally hundreds of samples might be needed at each deposit to obtain a reliable estimate of the beryllium content. Many of the localities visited are so isolated that only a few samples could be removed conveniently. In deposits consisting of alternating lay- ers of many types of material, a composite sample of the whole would be of little value in determining the beryllium-bearing type; yet sampling each layer indi- vidually requires much time and care. It is doubtful that beryllium-bearing minerals are evenly distributed through the containing rock masses. A sample taken at a point where the concentration of such minerals is relatively high might indicate a potential ore body, whereas one taken a short distance away might contain no beryllium even though the differences between the two materials might not be distinguishable in the field. Both would give an erroneous impression of the average contents. For these reasons, many of the samples that were analyzed probably were not truly representative, and future sampling in the same localities may give sig- nificantly different results. Three general methods of sampling were employed. Grab sampling, which consists of gathering pieces of material at random, was used at large mine dumps and mill tailings ponds. Channel sampling, which consists of cutting continuous strips of rock along preferred lines, was done mainly in mine openings. Because of the time consumed in this method, it was employed in relatively few places. Chip sampling, in which chips are taken along preferred lines, was used in sampling large exposures. In active mining districts, samples of the mill prod- ucts were obtained wherever possible, as well as sam- ples of ore and waste rock from the operating mines. At abandoned mines, an attempt was made to obtain representative samples of the different types of material observed on the dumps. An effort was made in sam- pling rock types to include all significant varieties noted in the field. Many hand specimens of rocks and min- erals were collected for laboratory study in event the bulk samples proved to contain beryllium. The field program was designed to obtain informa- tion concerning the beryllium content of a variety of rocks and mineral deposits throughout the United States in the shortest possible time. The amount of time that could be devoted to detailed geologic mapping was therefore small. For the most part, when geologic maps were not available for areas where samples were obtained, sketch maps were made showing the more pro- nounced geologic and cultural features. Topography and geology of areas at Wind Mountain in the Cornu- das Mountains, Otero County, N. Mex., and Cave Peak in the Sierra Diablo, Culberson County, Tex., were mapped in detail by planetable. DETERMINATION OF BERYLLIUM SPECTROGRAPHIC ANALYSIS The spectrographic method appears to be the most reliable for quantitative determination of small amounts of beryllium in rocks and minerals. A gen- eral discussion of the method is given by Peer (1948), and the application of the method to ore samples has been investigated by Marks and Jones (1948). The lower limit of accurate spectrographic determinations is in the range 0.005 to 0.0001 percent BeO. The equip- ment required is expensive and complicated, and trained technicians are needed to interpret the results. Spectro- graphic analyses of samples collected in the present in- vestigation were made in part by the Geological Survey laboratories, and in part by the National Spectro- graphic Laboratories, Cleveland, Ohio, and Strock Lab- oratories, Inc., Saratoga Springs, N. Y. 6 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES GRAVIMETRIC AND VOLUMETRIC ANALYSIS Beryllium as a trace constituent in rocks and min- erals cannot be determined quantitatively by gravimetric or volumetric methods of analysis, as the lower limit for BeQ of these methods is approximately 0.01 per- cent. Beryllium will generally be precipitated with aluminum unless special precautions are taken, and in many analyses it has been calculated with that metal. The problem of separating beryllium and aluminum has been a challenge to analytical chemists for many years, as is indicated by the extensive literature on the sub- ject. Special techniques must be employed also in the removal of iron, lest some beryllium be lost in the proc- ess. Any quantitative separation of beryllium should be verified by spectrographic analysis of residues. A gravimetric method for determining beryllium in rocks and minerals containing a few hundreds of 1 per- cent of the metal was developed by Stevens and Carron (1946). The new method separates beryllium from aluminum by a sodium carbonate fusion of their phos- phates and leaching with water. Various methods for removal of iron were studied, and the cupferron method was found to be most satisfactory. COLORIMETRIC AND FLUORIMETRIC ANALYSIS Colorimetric analysis is based on the reactions of cer- tain elements with dye reagents to produce colored or fluorescent compounds in solution. Many of the reac- tions are very sensitive and thus applicable to analysis for beryllium. A comprehensive treatment of the sub- ject is given by Sandell (1944). Several metals, includ- ing zinc, lithium, the rare earths, thorium, and calcium, react with certain of the reagents commonly employed in colorimetric tests for beryllium. Other elements such as iron, magnesium, manganese, and aluminum form flocculent hydroxides that cloud the solution and ab- sorb beryllium and the color reagent. Procedures for dealing with interfering ions differ according to the method of analysis employed, but in general they may either be eliminated from the solution or rendered harm- less by adding appropriate reagents. Special methods for removal of iron from the test solution have been de- scribed by Hillebrand and Lundell (1929, p. 110-111) and Sandell (1949, p. 93). The two types of color reagent that have been most used in beryllium determination are morin and the anthraquinones. Of the latter, quinizarin (1-4-dihy- droxyanthraquinone) and quinalizarin (1-2-5-8-tetra- hydroxyanthraquinone) are the most popular. Quini- zarin-2-sulfonic acid (1-4-dibhydroxyanthraquinone-2- sulfonic acid) has also been used (Cucei and others, 1949). Quantitative methods for each of the reagents have been rather carefully worked out. Comparative characteristics of the methods are shown in table 1 and detailed procedures are given in the publications cited. TaBus 1.-Comparison of quinalizarin, quinizarin, and morin methods for determination of beryllium in rocks and minerals Quinalizarin Quinizarin Morin Visual reaction ._.. Blue Jake_-.c.. ~. Red fluorescent Yellow-green fluorescent solution. Light conditions... . Daylight.........l..2.......s.. Ultraviolet (8,650 A).___________ Ultraviolet or sunlight. pH condition____._._._ ~-0.5N NaOH --. S% -Q0.3N NaOH (pH 11.5)1._..._. 0.01 to 0.1N NaOH. Sensitivity 1________ 0.5 :ppm 0.05 ppm Be.--.:-:............ 0.001 ppm Be. Interfering ions.... Zn, Mg, Zr, Th, rare earths_____. gap rans cena aas ge o Li, Ca, Zn, Sc. Remarks.____..__:; Least sensitive, best at high pH.. Most specific, color stable, tested Most sensitive, least specific, worst on all ores. at high pH, color fades, tested on all rocks. References......... Sandell, 1944, p. 153-154; Feigl, Rienacker, 1932; White and Lowe, Sandell, 1944, p. 152-153; 19402, 1939, p. 119-121; Fischer, 1928. 1941; Fletcher, White, and 1940b, 1949. Sheftel, 1946; Zermatten, 1933; Fletcher and White, 1946; Underwood and others, 1947.2 ' Stated in terms of minimum parts per million Be in test solution. 2 Underwood, A. L., Neuman, W. F., and Carlson, A. B., 1947, Determination of small amounts of beryllium by fluorescence measurement: U. S. Atomic Energy Comm., MDDC 941, 17 p. The morin reaction is the most sensitive of the three tests and, unlike other fluorescent methods, the fluores- cence may be observed in daylight. A disadvantage is the large number of interfering ions that must be eliminated. Though apparently suitable for rocks, this method may have application in testing ores. Quini- zarin gives a less sensitive fluorescent test than morin and requires the use of an ultraviolet lamp. Its chief advantage is that few ions interfere with the test, and therefore it is probably of greater use in testing of ores and all types of rocks than are other reagents. The quinalizarin test, like most other colorimetric methods, is of much lower sensitivity than fluorimetric reactions. However, only simple laboratory equipment is required in the procedure and most interfering ions may be elim- inated without difficulty. - Several other reagents have been found to give color reactions with beryllium but have not been adapted for DETERMINATION OF BERYLLIUM rg trace analysis of rocks and minerals (Kolthoff, 1928; Feigl, 1939, p. 121; Kulesar, 1943; Aldridge and Lid- dell, 1948; Underwood and Neuman, 1949; Kassel and Neuman, 1950). Most of the reagents used in colori- metric and fluorimetric analysis for beryllium may also be used in making qualitative spot tests. Reasonable precautions must be observed, even in qualitative work, in ridding the test solutions of ions which may ixfierfere with the results, and quantitative determinations may be carried out with slightly more effort, MINERALOGIC METHODS Beryllium in rocks may be determined by finding the amounts of beryllium minerals present and their beryllium contents. Commonly the BeO content of the mineral or minerals is determined by one of the meth- ods discussed above, though optical determinations are possible for some species. For accurate results the average of several determinations must be taken, Min- eral percentages by volume are determined by petro- graphic methods. Techniques employed with the more common beryllium minerals are discussed below. BERYL Beryl crystals, if large, generally may be recognized by their crystal form, hardness, and color ; some beryl, however, is white and easily confused with quartz or feldspar. Beryl in small crystals or fragments in a ground sample may be recognized microscopically, but identification is not always certain, for quartz and apatite have similar optical properties and crystal form. Once beryl has been recognized, its proportion in the rock may be found by one of the ordinary methods of volume, area, line, point, or grain counting, subject to the statistical restrictions of the method employed (Krumbein and Pettijohn, 1988, p. 465489). Because the specific gravity of beryl is about that of its usual gangue, quartz, its volume proportion is approximately equal to its weight proportion. The beryllia content of beryl ranges from 10 to 14 percent, varying inversely with the alkali content. The alkali content of the beryl may be determined by meas- uring the ordinary refractive index by the immersion method and referring to an empirical curve (Winchell, 1951, p. 464). In pegmatites the beryllium content of beryl may vary within a single pegmatite, or even within a single unit (Cameron and others, 1949, p. 69). No such variation has yet been discovered in veins, but relatively few analyses of vein beryl are available. Mineralogical calculation of beryllium in beryl de- posits has so far been applied only to pegmatites (Han- ley and others, 1950, p. 12). HELVITE GROUP In some districts, such as the Victorio Mountains and Carpenter districts, New Mexico, the Silverton district, Colorado, the Butte district, Montana, and the Rock- port area, Massachusetts, minerals of the helvite group commonly may be recognized by their crystal form and color. In the Iron Mountain district, New Mexico, and at places in some of the other districts just men- tioned, helvite is easily confused with garnet of the same shade of yellow or red. Some danalite and garnet in the Iron Mountain district were so intimately inter- grown that identification was especially difficult (Jahns, 19442, p. 57-58). A stain test developed by Gruner (1944) has proved useful if helvite is admixed with garnet. The proportion of helvite is determined by methods similar to those used for beryl. If the gangue is garnet, the volume proportions nearly equal the weight propor- tions. The theoretical BeO content of helvite ranges only from 12.5 to 13.5 percent (Glass and others, 1944, p. 182). In the absence of a chemical analysis, a value of 12.8 +0.9 percent BeO may be assumed. More than one mineral of the helvite group may be found in the same deposit," and this possibility must be considered in evaluating the beryllium content. Mineralogical calculation of beryllium has been ap- plied by Glass (Jahns, 1944a, p. 63, 77) to the Iron Mountain helvite deposit. OTHER MINERALS Other beryllium minerals have not been found in sufficient quantity to make their quantitative deter- mination important. - Beryllium-bearing minerals such as idocrase, garnet, axinite, aegirite, and nepheline have a content of beryllium that ranges from more than 3 percent BeO to below the limit of detection. Correlation between physical properties and beryllium content is uncertain for these minerals, and no data have been gathered on their probable ranges of beryl- lium content within a given deposit or rock type. The two minerals of highest extraneous beryllium content are allanite and idocrase, both of which con- tain such a diversity of elements that correlation of physical properties with beryllium content is extremely difficult. Gideke (1938) has achieved some success in correlating the optical properties of idocrase with its highly variable composition. However, some half- dozen types of isomorphous substitution were found to have a marked effect on the optical properties, and a reliable criterion for determining the presence of be- ryllium seems improbable. If either idocrase or al- ~ ifron Mountain, N. Mex. (Jahns, 19448, p. 56-58) ; Bartlett, N. H. (Glass and others, 1944, p. 185); and Cornwall, England (Miers and Prior, 1892, p. 11). 8 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES lanite occurs in a deposit containing helvite or beryl, it may be expected to be beryllium-bearing. In each of the three helvite deposits where idocrase has been found and analyzed, it contained at least 0.2 percent BeQO. In such deposits a mineral count of beryl or helvite will give a BeQO content below the true value. A mineral count of all the recognizable beryllium minerals may miss a substantial quantity of beryllium occurring in fine-grained or unknown species. This was the experience of Glass and Lemke with the Iron Mountain, N. Mex., tactite (Jahns, 1944a, p. Ti-78), and of Holser with the Victorio Mountains, N. Mex., tactite during the present investigation. However, the beryllium content determined from beryl or helvite counts could be of more economic significance than that given by chemical or spectrographic methods if the trace quantities of beryllium in the minerals associated with the beryl or helvite were not recoverable. RADIOMETRIC METHODS Beryllium is an efficient producer of neutrons when excited by high-energy gamma radiation. It shares this property with H* and several other atoms, but the energy threshold for the beryllium reaction happens to be lower than for any other element. The reaction was experimentally applied to the mechanical sorting of beryl (Gaudin and others, 1950), and the data ob- tained in these experiments allow a preliminary calcu- lation of the sensitivity of the reaction for the assay of beryllium in rocks. The gamma-ray sources used in the published experi- ments were a Van de Graaf generator and radium (Gaudin and others, 1950, p. 496). The recently avail- able artificially radioactive antimony may be more de- sirable for field determination of beryllium, despite its short half-life. It decays according to the following equation : 60 days Sb -> Te#-6;, Mev-|yi.; Mey The gamma radiation is of sufficient energy to excite beryllium, giving 2.10° neutrons per curie per gram of beryllium at 1 em. (Russell and others, 1948). Sb! possesses an advantage over Ra* in the analysis of nat- ural materials, because it gives only a very small num- ber of neutrons from H*. The neutrons may be slowed in a moderator, such as paraffin, and detected by stand- ard procedures. Preliminary calculations, including al- lowance for efficiency and background, indicate a limit of detection of 0.00X (percent BeOQ times curies of Sb"), This method has some promise for semiportable field equipment, as it would be highly specific, independent of the state of beryllium, fast, and simple. However, there are several disadvantages. Initial expense would be moderate but operating expense would include the maintenance of a supply of Sb'***, which has a rather short half-life. Safety and waste-disposal of the source required to detect small amounts of BeQ would be problems. MINERALOGY OF BERYLLIUM CRYSTAL CHEMISTRY OF BERYLLIUM MINERALS Most beryllium minerals are silicates, many of which are structurally complex. The commonly associated ele- ments are aluminum and the metals of the alkali and alkaline-earth groups, together with fluorine, water, and the hydroxyl ion. With few exceptions, iron and mag- nesium are rare constituents. Other mineral groups, in- cluding oxides, carbonates, phosphates, and borates, are sparsely represented, but sulfides, halides, and related compounds are notably lacking. The tendency for beryllium to affiliate itself with the silicates and oxygen salts in preference to the sulfides and halides is best ex- plained by the marked difference in crystal chemistry of these compounds. Full treatment of this subject is beyond the scope of this report. However, the prin- ciples involved are thought to have an important bear- ing upon the nature and occurrence of beryllium min- erals and thus to merit the following brief discussion. Beryllium has a relatively small ionic radius, is strongly electropositive, and is found only in tetra- hedral coordination in erystal structures. As a result of these properties, it favors combination with anions that are not easily polarized, forming crystal bonds of the ionic or semi-ionic type. Stable combinations of beryllium with sulfur, which is readily polarized, are not to be expected. Similarly, chlorine, bromine, and iodine form structures which, except for the alkali chlo- rides, tend to approximate the sulfide type and are not likely to contain beryllium. Fluorine vigorously resists polarization but, because of its large ionic size does not favor tetrahedral coordination with beryllium. The most stable combination of beryllium is with oxygen, which is not readily polarized and, which, though com- parable in size to fluorine, will permit bonds of semi- ionic type involving some electron sharing. Such bonds result in relatively close packing of four oxygen ions around the small beryllium ion and permit the required spacing of beryllium ions in the structure. The oxide, bromellite, though rare, is thus a stable mineral com- pound. The silicate minerals are most favorable for beryl- lium occurrence. The complex structural arrangement and chemical composition of these minerals give greater opportunity for meeting the four-fold coordination re- quirement of beryllium. Even here many combinations MINERALOGY OF BERYLLIUM OQ which fit the ordinary laws of valency are structurally incompatible. Whereas beryllium is known only in tetrahedral coordination in oxyminerals, aluminum, iron, magnesium, and other elements are capable of either four-fold or six-fold coordination. Such ele- ments therefore have a considerable advantage over beryllium in meeting structural requirements in silicate minerals. Even if beryllium were present in concentra- tion equal to that of these elements, a condition which is rare in nature, it would be at a loss in competing with them for positions in crystal lattices. Though oxysalts of beryllium occur as minerals, they are not common. In the oxyradicals, oxygen atoms are closely grouped around small atoms such as carbon, ni- trogen, and phosphorus; and bonds within the radicals are mainly covalent. Because the bonds between beryl- lium and oxygen are mainly ionic, the beryllate radical is unstable in nature and not found in minerals. Bonds between beryllium ions and the large oxyradicals are of a weak ionic type and the resulting beryllium nitrate, carbonate, and phosphate also have poor stability under natural conditions. In the presence of water, especially at low tempera- tures, hydrogen has considerable influence on the rela- tions of beryllium and oxygen. The hydroxyl ion is deformed by the charge of the beryllium ion and, ac- cording to the theory developed by Wickman (1944), the resulting deformation may allow formation of hy- droxyl bonds and precipitation of beryllium hydroxide. This is thought to be of considerable importance in the occurrence of beryllium in sedimentary rocks. Many minerals contain beryllium in solid solution, though rarely in significant amounts. That ionic size, rather than valency, is the controlling factor in isomor- phous substitution is now commonly accepted. Thus beryllium may replace ions or atoms of comparable size in crystal structures but is not likely to replace those of substantially different ionic radius. Because of the dis- crepancy in ionic size, the substitution of beryllium for most of the more common metals is not to be ex- pected in appreciable amount. The best possibilities for substitution are with ions such as Cré, P", S*, and Si, which are of about the same size as Be*. Not only are these ions, except that of silicon, compara- tively rare, but all have valences ranging from four to six, whereas the valence of beryllium is only two. Other ions of some of these elements have lower val- ences, but their radii are considerably larger than that of the beryllium ion. Although difference in valence does not prohibit substitution, the ions of higher charge will in general be somewhat more stable in the struc- ture than beryllium (Goldschmidt, 1934, p. 385) ; also the interchange of ions is subject to the condition that the positive and negative charges must balance. Excess charges may be balanced by adding ions to the structure. Such complex substitutions are well known.: in amphiboles, micas, and clay minerals. As an ex- ample, Rankama and Sahama (1950, p. 126) theorize that the small content of lanthanum sometimes present. in potassium feldspar is a result of the substitution of La® for K+ simultaneously with Be* for Si*. Not only must the combined charges of the substituting ions bring about electrical neutrality in the structure but their sizes and coordination numbers must be such that they will fit into the spaces provided by the ions replaced. The difficulty of finding proper combinations is im- measurably increased when the disparity of valences is greater, so despite the greater difference in ionic size, Be* is more likely to substitute for Si* than for S4, Cr, or P". Presumably beryllium ions or atoms may fill inter- stices of proper size in certain crystal lattices without actually substituting for other ions. In this connection the small ionic radius for beryllium would seem a dis- tinct advantage. However, the difficulties inherent in isomorphous substitution would not be entirely obviated in this process, and it is doubtful that significant amounts of beryllium could be thus accommodated ex- cept in minerals where vacant oxygen tetrahedra exist, as in idocrase. On the whole, isomorphism does not promise to pro- vide minerals of even moderately high beryllium con- tent except under special conditions. Undoubtedly it is a means by which much beryllium is dissipated among silicate minerals as a trace constituent. Throughout the foregoing discussion the matter of ion concentration, or availability, has been largely ne- glected. As pointed out by Osborn (1950), the con- centration of a given element in a particular geologic environment has much to do with the amount of that element contained in the minerals that form. In the early stages of basaltic magma erystallization the con- centration of beryllium is low, and it is not a serious. competitor to the more common cations which are more readily incorporated into the structures of the ferro- magnesian silicates and plagioclase. It thus tends to be concentrated in the late magmatic residue where op- portunities for the formation of minerals in which beryllium is a necessary constituent reach their maxi- mum. Silicate minerals that form during the late mag- matic and early hydrothermal stages of igneous activity probably remove most of the beryllium. Sulfur, the oxyradicals, and to some extent the halogens tend to be concentrated in later hydrothermal fluids and combine with metals to form the common ore and gangue min- 10 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES erals. Not only are the structures of these minerals un- favorable to beryllium occurrence, but the concentration of beryllium in the ore fluid probably is low, most of it having gone into previously formed minerals. Pauc- ity of beryllium in ore deposits that formed at moderate or low temperature is, therefore, to be expected. Theoretical considerations thus indicate that, because of the peculiar structural and chemical properties of beryllium, minerals in which beryllium is a necessary constituent are few. - These minerals are most likely to cceur in rocks believed to have formed during the tran- sition from magmatic to hydrothermal activity. The number of potential beryllium ore minerals is, there- fore, not large and their geologic environments are restricted. These principles, though not without ex- ception, are in accord with, and tend to substantiate, conclusions previously drawn from field observations. BERYLLIUM AS AN ESSENTIAL CONSTITUENT IN MINERALS Minerals in which beryllium is an essential constituent are described in table 2. Although the list is an im- posing one, many of these minerals are rare, and some are found in only one or two localities. Knowledge of physical and chemical conditions in nature, is not ade- quate to explain these rare occurrences. Beryl, helvite, bertrandite, chrysoberyl, and phenakite are not only the most common minerals of beryllium, but actually ac- count for nearly all mineralogical occurrences as well as all probable ores of beryllium. All can occur in de- posits other than pegmatites. The chrysoberyl (BeAl,Q.) structure is similar to that of fayalite and has been described by Bragg and Brown (1926). Although the possibility of isomorphic variation in the aluminum or beryllium content is sug- gested by artificial melt studies (Geller and others, 1946, p. 289), the only variation found in natural chrysoberyl has been the substitution of small amounts of ferric iron for aluminum, and ferrous iron for beryllium (Palache and others, 1944, v. 1, p. 419). Chrysoberyl occurs in some pegmatites and in at least one it constitutes beryl- lium ore (Hanley and others, 1950, p. 103). It is found also in aluminous schists commonly associated with peg- matites, as in the Ural Mountains (Fersman, 1929, p. 94) and in New York (Palache and others, 1944, v. 1, p. 721). None was found during the present investiga- tion. Tasur 2.-Minerals in which beryllium is an essential constituent [Key to abbreviations: isom.-isometric; tetr.-tetragonal; hex.-hexagonal; trig.-trigonal; orth.-orthorhombic; mono.-monoclinic; H-hardness Moh scale; G-specific gravity; F-fusibility; Cl-cleavage form; N-index of refraction; N,-index of refraction for the ordinary ray; Ne-index of refraction for the extraordinary ray; Ny-index of refraction for the intermediate ray; B-birefringence; 2V-optic axial angle] Mineral Chemical composition Percent BeOQ Description Occurrence ..... CasBesAl(OH);S8igO0g4H20.. . 6.2 Tetr., pyramidal; vitreous; color- Pyrometasomatic, with mag- less; H, 5.5; G, 2.9; N,, 1.64; N,, netite; very rare. 1.637; B, 0.010. Barylite....... 15. 4-15. 8 Orth., platy; greasy; white; insol- Pyrometasomatic, New Jer- uble; C1, 001, 100; H, 6-7; G, 4.0; sey; very rare. F, 1; N,,, 1.08-1.70; -B,.0.013; (+)2V, 65° to (-)2V, 65°. Bavenite_____.. Ca, BeAlsS8iqOz4.H2O. ___ ___... 3. 0- 7.7 Orth., fibrous, prismatic; white; H, Granitic pegmatite, Italy; 5.50, 2.7; Ny,. 1.58-1.50;, B, very rare. 0.004-0.0007; (-)2V, 47°. Bertrandite.._.. 39. 6-42. 6 Orth., tabular, prismatic; vitreous; Granitic pegmatite and feld- colorless, yellow; insoluble; Cl, spathic veins; widely dis- P91, 110,100; H;, 6; (1, 2.6; F, 7; tributed in small amounts. Ny, 1.61; B, 0.023; (+)j2v, 744. Be:sAls(B10g)46.....1.... _. 10. 0-14. 0 Hex., prismatic (vert. striae), vit- Granitic - pegmatite, high reous; green (rarely white, pink, temperature veins; widely yellow) ; insoluble; CI, 001 (poor); distributed. Alters to kao- G, 262.8: M;. 1p7- - linite. 1.60; N., 1.56-1.59; B, 0.004-0.008. Beryllonite.__... . 19.8 Orth., short prismatic; vitreous; Granitic pegmatite, Maine; colorless, white, yellow; soluble; rare. CI, 001, 100; H, 5.5-6; G, 2.8; F, 5; Ny, 1.56; B, 0.01; (-)2V, 67°. Bityite..:.-..« Ca,(Li, Be)4Als- 2. 8- 8.1 Pseudohex., minute plates; white; Granitic pegmatite, Mada- [(8i, Al)aOuhs (OH)». insoluble; Cl, 001; H, 5.5; G, 3.0; gascar; rare. F, easy; Ny, 1.63; B, 0.02; (-)2V, small. Bromellite ___.. s. nre l nee Po eee aeg 100.0 Hex., prismatic; white; insoluble; Pyrometasomatic, Sweden; S}, 10710; #,°0; (1; 3.0; -N,, 1.72; very rare. ss 1973. ° Chkalovite___.. NapeSizO;-. _.. 12. 7 Orth., colorless; H, 6; G, 2.7; soluble; Syenitic pegmatite, U.S.S.R; CL; Ny, 1.55; (+) 2V, 78°. very rare. Chrysobetyl...._. 16. 9-19. 7 - Orth., tabular, twinned crystals; Granitic pegmatite, schist, vitreous; green, yellow, brown, red; Cl, 110; H, 8-9; G; 3.7; F, 7; Ny, 1.75; B, 0.009; 2V, variable. placers; uncommon. MINERALOGY OF BERYLLIUM I4 Tasu® 2.-Minerals in which beryllium is an essential constituent-Continued Key to abbreviations: isom.-isometric; tetr.-tetragonal; hex.-hexagonal; trig.-trigonal; orth.-orthorhombic; mopo.—m0noclinie; H-hardness Moh scale; G-specific gravity; F-fusibility; Cl-cleavage form; N-index of refraction; N,-index of refraction for the ordinary ray; N&-index of refraction for the extraordinary ray; Ny-index of refraction for the intermediate ray; B-birefringence; 2V-optic axial angle] F, 6; Ny, 1.72; B, 0.01; (-)}2V, 83°. Mineral Chemical composition Percent BeQ Description Occurrence ¥EM Epididymite-.. HNaBeSi;zQOs..:-...-....... 10.6 Orth., basal plates; vitreous; white; Syenitic pegmatite, Green- pearly insoluble; Cl, 001 and 010; land; rare. 0G, 2.6; .F., 3; Nyy. 1.54; B, 0.002; (+) 2V, 23°. : .._ 16. 9 Mono., prismatis; vitreous; color- Granitic pegmatite, chlorite less, green, blue, white; insoluble; schists, placers; rare. C1, 010; H, 7.5; G, 3.0-4.0; F, 5.5; Ny,, 1.655; B, 0.02; (+) 2V, 50°. 10. 6-11. 1 Mono., basal plates; vitreous; white; Zircon syenitic pegmatite, nearly insoluble; CI, 001; H, 6; Norway; rare. (4,-2.5; F, 5; Ny,, 1.55; B, 0.006; (+) 2V, 30°. Gadolinite _.... BesYsFeSiOm-.....-..-...= 5. 5-13. 2 Mono., prismatic; vitreous; black, Granitic pegmatite, gener- greenish, brown; gels HCI; Cl, ally with fluorite; uncom- none; H, 7; G, 4.0-4.6; Ny, 1.78; mon. B, 0.01; (+), 2V, 85°. Hambergite.... Bes(OH)BO;:.-_..___.___.. 36.7 Orth., prismatic; vitreous; gray- Granitic and syenitic pegma- white; insoluble except in HF; tites, Norway and Mada- CJ, 010 and 100; H, 7.5; G, 2.3; gascar; very rare. 57,07; Ny,, 1.59; B, 0.074; (+) 2V, Harstigite..__.. (Ca, F)... 11.2 Orth., short prismatic; vitreous; Pyrometasomatic, Sweden; colorless; soluble in HCI after ig- very rare. nition; C1, none; H,,5.5; G,: 8; N,, 1.68; B, 0.005; (+) 2V, 52°. HELVITE GROUP Helvite.......- Mn, 10. 5-15. 0 Isom., tetrahedrons, spherical masses; Pyrometasomatic deposits; vitreous to resinous; yellow, red, rhodonite veins, granitic brown; gels in HCI; CI, 111 (poor) ; and syenitic pegmatites; H, 6; G, 3.2-3.4; F, 3; N, 1.783-1.75. uncommon. Paralite"_..".. 12. 7-13. 8 Isom., octahedrons, massive; red, Granitic pegmatite, pyro- brown; H, 6; G, 3.3-3.5; F, 3; metasomatic deposits; N, 1.75-1.77. rare. Genthelvite_.__. 12. 6 Isom., rose red, brown; H, 6; G, 3.6; Pegmatite, Colorado; very y 1.10. rare. Herderite. ...... 15. 0-15. 8 Mono., prismatic; vitreous; yellow- Pegmatites, Maine; very ish to greenish; soluble in acid; rare. C1, 110 (poor) ; H, 5; G, 3.0; F, diffi- cult; Ny,, 1.61; B, 0.029; (-)2V, 74°. Kolbeckite(?)._. Hydrous Be, Ca, Al, Si phos- 8.7 Mono., short prisms; blue to gray; Quartz-wolframite vein, Ger- phate, poorly defined. C1, 010; H, 3.5-4.0; G, 2.4. many; very rare. Leucophanite... (Ca,Na)Be Si@(O,0H,F);.__. 10.0-12. 4 Orth., basal plates, massive, col- Syenite pegmatite, Norway; umnar; vitreous; white, green, very rare. yellow; insoluble; CI, O01, 010; H; £; G, 5;.F.. 0; N,, 1.59; B, 0.027; (-)2V, 39°. Meliphanite._.. - (Ca, Na)2Be(Si, Al)s(O, F);--. 9.8-14.0 Tetr., obtuse pyramidal or platy; Syenite pegmatites, Norway; vitreous; yellow to reddish; insol- very rare. uble; Cl, 001; H, 5-5.5; G, 3; fuses with intumescence; N,, 1.61; N., 1.59. Milarite. ...-. KCa,BeqAlsSizOs0. H20O.-- _ -- 5.0 - Hex., prismatic; vitreous; pale green, Granite, Switzerland; very colorless; insoluble; no cleavage; rare. H, 5.5-6; G, 2.6; F, 3; N.,, N., 1.53; B, 0.001-0.003. Phenakite.___.. 44. 0-45. 6 Trig., rhombohedral or prismatic; Granitic pegmatites, high vitreous; colorless, yellow, rose, temperature veins; rare. brown; insoluble; CI, 1120; H, 7558; G, 3.0; F, 7; N., 1.654; N., 1.670. Rhodizite__.... (Na, K);LisALBesB1002:(?) - - - 9.0-15. 1 Isom., dodecahedrons; translucent; Pegmatite, U.S.S.R., Mada- white or yellow; insoluble; Cl, 111 gascar; very rare. (poor); H, 8; G, 3.4; F, 7; N, 1.69. Swedenborgite _. NaBeqSbO;-______________- 35. 3 Hex., short prismatic; colorless; yel- Pyrometasomatic deposit, low; insoluble; CI, 0001; H, 8; G, Sweden; very rare. 4.8> N.,, 1:77, Ns, 1.77; B; 0:002. Tengerite._._.... Hydrous Y, Ca, Be carbonate. 9.8 Fibrous, powdery; dull; white; sol- Granitic pegmatite as alter- uble with effervescence; G, 3.1; ation product of gadoli- lNy, 1.57-1.63;B,0.02-0.03; (-)2V, nite, Texas; very rare. arge. Trimérite...... BesMnsCa(Bi04)3.._......_.. 17. 1 - Mono., tubular prisms; pink; soluble Pyrometasomatic, Sweden; in H’Cl; C1, 0001; H, 6-7; G, 3.5; very rare. 12 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES The phenakite (BeSiO.) structure according to Bragg and Zachariasen (1980) consists of linked tetra- hedra with silicon and beryllium at their centers. The structure is similar to that of willemite and a small amount of willemite is needed as a seeding agent in pro- ducing synthetic phenakite (Morgan and Hummel, 1949, p. 252). Phenakite occurs in small quantities in pegmatites, but rarely is found in those containing chrysoberyl. It is an associate of beryl in a few granites containing segregations of aplite and occurs rarely in beryl-bearing quartz veins. None was discovered in the current investigation, but it has previously been de- seribed from veins at Irish Creek, Va. (Koschmann and others, 1942, p. 281-282) and Mount Antero, Colo. (Switzer, 1989, p. 789). Beryl (BesAl;(Si0;)«) is uncommon among silicates as an example of a sixfold ring structure of four-co- ordinated silica groups (Bragg and West, 1926). The groups are tied together by beryllium in four-coordina- tion and aluminum in six-coordination. Beryl is variable in composition, ranging from 10 to 14 percent BeO (the formula content is 14 percent). Alkalies and alkaline earths, principally sodium, con- stitute as much as 4 percent of many beryls, and con- stitutional water may amount to 2.7 percent. The de- crease of beryllium content might be structurally cor- related with either the addition of an alkali atom to the empty position in the center of each silicate ring, or with the substitution of hydroxyl for oxygen in part of the ring itself. Both systems have been found in other silicates; * sufficient analyses are not yet available to determine which is more important. Theoretically, the type and amount of substitution in beryl should be closely related to the mode of occur- rence. Beryl formed as a late magmatic product should contain less beryllium than that formed earlier, because of increase in alkali content of the magma as differen- tiation progresses. The abundance of water in the pre- forming fluid should result in a further reduction of beryllium in vein beryl. Accordingly, the alkali con- tent of beryl might be expected to increase during peg- matization and, in general, the beryllium content of beryl should be higher in igneous rocks than in vein deposits. The few analysis of nonpegmatite beryl show, however, that the average BeO content does not appear to be appreciably different from that of beryl in peg- matites. The optical data on nonpegmatite beryl indi- cates that the index is higher, and therefore the beryl- lium content probably lower in tungsten-bearing veins than in molybdenum- and tin-bearing veins (Adams, 1953, p. 117). 2 Na in amphibole: Warren (1929, p. 42) ; OH in garnet: McConnell (1942, p. 458-460). Beryl is the most common beryllium mineral in beryl lium-bearing veins. The vein occurrences are tabulated and discussed by Holser (1953, p. 604) and by Adams (1953, p. 114-117). Beryl also occurs less commonly as an accessory mineral in granitic rocks and in schists, generally associated with pegmatites. The known oc- currences in nonpegmatite rocks of the United States are discussed in this report. Helvite and its isomorph ((Mn, Fe, Zn),BesSizO:1»8) have a three-dimensional framework of oxygen tetra- hedra similar to that of sodalite. Beryllium occupies the position normally given to aluminum in such struc- tures, and this allows the presence of the divalent metals in place of sodium (Barth, 1926, p. 40). The chemical composition and physical properties of the helvite group are summarized by Glass, Jahns, and Stevens (1944), who list many helvite localities. In addition to the pegmatite occurrences at Amelia, Va., Cheyenne Canyon, Colo., Rockport, Mass., Langesund- fiord, Norway, Miass, U. S. S. R., and Mount Francisco, western Australia, helvite has been found in pegmatites at Rincon, Calif. (Murdoch and Webb, 1948, p. 170), Walrus Island, Northwest Territory, Canada (Hoff- man, 1901, p. 15), and Ipe', Minas Gerais, Brazil (writ- ten communication, E. R. Swoboda). In common with phenakite and beryl, minerals of the helvite group are found rarely in small rather fine-grained segregations in granite (Fischer, 1942). Most helvite occurs in veing and pyrometasomatic deposits. Occurrences in the United States are described in detail in this report. BERYLLIUM AS AN ACCESSORY CONSTITUENT IN MINERALS The minerals that are known to contain beryllium as an accessory constituent are listed in table 3, together with some of their physical properties and their modes of occurrences. The range of beryllium content re- ported for these minerals is also indicated, although the accuracy of most of the figures is difficult or impossible of evaluation. Aside from the usual analytical diffi- culties, most reports in the literature give no informa- tion about what precautions were observed against in- clusions of other beryllium minerals. Indeed, even with detailed microscopic examination of the sample, one cannot be certain of its nature, as only a few mi- nute grains would be necessary to give the small amounts of beryllium detected by spectrographic analysis. The recovery of beryllium by known hydrometal- lurgical or similar methods from most minerals in which beryllium is dispersed as an isomorphous. con- stituent is not possible, but some recovery may be pos- sible from very low grade material containing inclu- MINERALOGY OF BERYLLIUM 13 Tamm 3.-Minerals in which beryllium may be am accessory constituent {[Key to abbreviations: isom.-isometric; tetr.-tetragonal; hex.-hexagonal; trig.-trigonal; orth.-orthorhombic; mono.-monoclinic; tric.-triclinic; H-hardness Moh scale; G-specific gravity; F-fusibility; C1-cleavage form; N-index of refraction; N,-index of refraction for the ordinary ray; Ne-index of refraction for the extraordinary ray; Ny-index of refraction for the intermediate ray; B-birefringence; 2V-optic axial angle] Approzimate mazimum Mineral Chemical composition percent BeQ Description | Occurrence Amphibole | group: | Arfvedsonite. - Nas(Fe,Mg),FeSisO»n(OH):;--_-- 0. OX Mono., prismatic; vitreous; black Alkalic igneous rocks; un- to deep green; insoluble; Cl-110; common. H-6; G-3.5; F-2; Ny-1.69; B-0.015; (-)2V-variable. Glaucophane. - Na;MgsAl;SigOqq(OH);-------- . O01 Mono., prismatic; vitreous; blue; Schists; uncommon. insoluble; Cl-110; H-6; 3.0-3.1; N,-1.63; B-.019; (-) 2V-small. Hornblende.. Ca;(Mg,Fe)sSigOa(OH):------- . 006 Mono., prismatic; vitreous; green to Igneous and metamorphic black; Cl-110; H-5.6; G-2.9- rocks; very common. 3.4; N,-1.61-1.71; B-0.02-0.03; (-)2V-large. Apatite...:.... OH) ;(PO-AsO4)s- - - - .:Of Hex., prismatic; vitreous; green, Widely distributed igneous white; soluble; H-5; G-3.2; rocks, pegmatites and sedi- CI-0001 ' imperfect; _ N,-1.00- mentary and metamorphic 631, N,-1.58-1.77; B-0.002- rocks; common. Axinite.....-.- H(Fe, Mn) Ca;Al;BSi4016--- - - - - Tric., wedge-shaped; vitreous; Pyrometasomatic and high- brown, blue, gray; insoluble; Cl- temperature veins; un- 112, 010, 180; H-7; G-3.3; common. F-2; N,-1.68-1.69; B-0.01; Cassiterite..... oc- en tr Tetr., short prismatic or pyramidal; - High-temperature veins and adamantine; brown or black; Cl- pegmatites, placers; com- 110; H-6-7; G-6.8-7.1; N.- mon. 1.99; N,-2.09. Chevkinite._... (Ca, Fe) (Ce, ¥, Di):(8i,Ti);0w--- _ 1. 9 Mono., vitreous; red-brown, black; Granitic pegmatite; rare. gels with HCI; Cl-none; H-5; G-4.3-4.6; F-4; N,-1.88-1.97; B-low, may be amorphous and isotropic. Chlorite........ (Mg, Fe, Al)s-4(8i, Al)0 &r Mono., lamellar; pearly; green; Cl- Schists and hydrothermally 001; H-1-2; G-2.6-2.8; N,- altered rocks; common. 1.58; B-0.003-0.007; (+)2V- small. Clay minerals: Tilite series... - K;(Al, Mg) (Si, Al).On(OH)» . 008 Mono., minute lamellae; white; Soils; very common. nH0. ~H-2; G-2.6; N,-1.57. Kaolinite . 005 Tric., minute pseudohexagonal plates, Hydrothermally altered group. vermicular groups common; white; rocks, soils; common. H-2; G-2.6; F-7; N,-1.56; B-0.006; (-)2V-20°%-55°. Montmoril- Al; ;(Na, Mg) 80 n(OH)». . O1 Mono., minute lamellae; CI-O001; Altered tuff, hydrothermally lonite nH;0. H-1.5; G-2.5-2.6, F-5 with altered rocks, soils; com- series. swelling; N,-1.50-1.60; B-0.025; mon. (-)2V-variable. 1.7 Mono., complex crystals; vitreous; Pyrometasomatic; rare. yellow, red; gels in HCI; CI-O001; H-6; G-8.2; F-7; N,-1.65; B-0.03; (+)2V-large. Epidote group: Car (AlL, Fe, Mn) O; Al(AlSig) Op-. tr Mono., prismatic or acicular; vit- Pyrometasomatic, metamor- reous; green to black; partially phosed limestones; com- decomposed by HCI; CI-O001; mon. H-6-7; G-3.3-3.5; F-3 (swells); N,-1.72-1.82; B-0.006-0.07; 2V-large. (Ca,Ce);0-Fe;0H-AlL (AL, Sig) O;. _ 5.5 Mono., tabular or acicular; subme- Accessory in acidic igneous tallic; brown to black; gels in HCI; rocks, gneiss, schist, mag- no distinct cleavage; H-6; G-4; netite iron ores; uncom- F-2.5 (swells); N,-1.65-1.78; mon. All beryllium ma- B-variable; (-)2V-large. terial from granitic peg- matite; rare. Eudialite_______- (Na, ___ __ . 005 Hex., rhombohedral; pink; gels in Nepheline syenite pegma- HCI; CI-001; H-5; G-2.8-3.1; tite; rare. F-2.5; uniaxial{+ or-; No, N- 1.59-1.64; B-0.00-0.01. Euxenite_____-- _ (¥,Ca,Ce,U,Th)(Cb,Ta,Ti);04._ . 05 Orth., massive; brilliant; brownish Pegmatite; rare. black; insoluble; CI-none; H- 6.5; G-4.8; F-7; isotropic (from alteration); N-2.06-2.26. 14 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TaBum 3.-Minerals in which beryllium may be an accessory constituent-Continued [Key to abbreviations: isom.-isometric; tetr.-tetragonal; hex.-hexagonal; trig.-trigonal; orth.-orthorhombic; mono.-monoclinic; tric.-triclinic; H-hardness Moh scale; G—sggcmc gravity; F-fusibility; Cl-cleavage form;*N-index of refraction; No-index of refraction for the ordinary ray; N«-index of refraction for the extraordinary ray; Ny-index of refraction for the intermediate ray; B-birefringence; 2V-optic axial angle} Approzimate marimum Mineral Chemical composition percent BeOQ Description Occurrence Feldspar group: Microcline . . .. 0. 04 Tric., short prismatic crystals; vitre- Granitic rocks, pegmatite, (microper- ous; white; CI-O01, 010; H-6; metamorphic rocks; very thite). G-2.55; F-5; Ny-1.52; common, B-0.007; (-) 2V-large. Piaglociase... . O1 Tric., tabular or prismatic; vitreous; Igneous rocks and pegma- white; C.-O001, 010; H-6; tite, metamorphic rocks G-2.6-2.70; F-5; N,-1.53- very common. All beryl- 1.58; B-0.01; 2V-large. lian material is albite from pegmatite. Fergusonite...._ _L . 74 Tetr., prismatic or pyramidal; sub- Pegmatite; rare. metallic; brown; soluble in HSO4; Cl-111; H-6; G-5.8; F-7; isotropic (from alteration) ; N-2.06-2.19. Fivorite. /'... Cars? rac- . sean . 000X Isom., cubic; vitreous; white, purple; Accessory in igneous rocks soluble in H&SQ,; Ci-111; H-4; and pegmatites; - wide- G-3.2; F-3; N-1.48. spread in veins and pyro- metasomatic deposits; common. Garnet CastAl FelsBhOs._-::. _c .CZ __. 12 Isom., dodecahedronai; vitreous; red, Pyrometasomatic; common. (grossularite- brown, yellow, green; Cl-none; andradite). H-6.7; G-3.1-3.4; F-3; N-1.74-1.79. : ~ MIAkS ._. ._ A tr Isom., massive, metallic, silver-white; Sulfide veins; rare. Cl-none; H-5.5; G-5.6-6.2. Homilite.._.... _ .L.______._____ 3. 0 Mono., basal plates; black; H-5; Syenitic pegmatites, - Nor- (G-3.36; F-2; geis in HC; N, way; very rare; beryliian -1.73;B-0.023;(+) 2V-80°®. variety highly alterea. Hyalotekite_... . 18 Orth. (?); vitreous; white; insoluble Pyrometasomatic deposits, in HCl; Cl-2 at 90°; H-5; Sweden; very rare. G-3.8; F-3; N,-1.96; B-0.003; (+) 2V-small. Idocrase Car(Al, Mg)1s8ig(O,0H,F) ;;... - 4.0 Tetr., prismatic; vitreous; brown, Pyrometasomatie deposits; (vesuvianite). green, blue; decomposed by HCi; common. Ci-110 (poor); H-6.5; G-3.4; F-3; N-1.71-1.174; N,&-1.70- 1.73; B-0.001-0.006 (may be biaxial, small 2V). Maucherite.... _ tr Tetr., square tabular crystals; metal- - Sulfide veins; rare. lic; reddish white; Cl-none; H-5; G-7.8; F-easy. Mica group: Biotite... K(Mg,Fe)3(AlSis) O1,{(OH)s. .._. . OX Mono., tabular; pearly; black; de- Igneous and metamorphic composed by H&SQO«,; CI-O001; rocks very common, H-2.5-3; - G-2.8-3.4; F-B; (Beryllium-bearing - sam- N,-1.56-1.69; - B-0.040-0.060; ples obtained from gran- (-) 2V-small. ite, pegmatite, and re- « lated rocks.) Leptdolite.... OX Mono., tabular; pearly; violet, yel- Granitic pegmatites and tin low; attacked by acids; Cl1-O01; H-2.4-4.0; G-2.8-8.3; F-1.5- 2.50; Ny-1.55; B-0.02; (--) 2V- 42 veins; common. Microlite ___. Nepheline.____. _._ Pyrophyllite KAls(AISiq) O1p(OH)g _ ___ __ (Na, ___ _. __ .msi nce A..suls og. Sate cect MasStQOie(COH)s . £20002 {Louise ip Mono., tabular; pearly; colorless, brown ; insolubie in acids; CI-001 ; H-2.5-3; G-2.7-3; F-6; N,- 1.58; B-0.036; (-) 2V-47°. Isom., octahedral; vitreous, brown, black; decomposed by H-5.5; G-5.5; F-7; N-1.93. Hex., tabular, prismatic; vitreous to greasy; colorless; H- 5.5-6; 6G-2.6; F-4; N,-1.54-1.55; N,-1.53-1.54; B-0.003-0.005. Hex., massive; metallic; pale red; Cl1-none; H-5; G-7.3-7.7. Mono., lamellar; pearly; white; CI-Q01; H-1; G-2.8; F-6; N,-1.59; B-0.048. Granite, gneiss, schist, peg- matite, hypothermal veins; very common. Granitic pegmatite; very rare. Sodic syenites; common. Sulfide veins; common. Metamorphic rocks; - un- common. MINERALOGY OF BERYLLIUM 15 TaBum 3.-Minerals in which beryllium may be am accessory constituent-Continued Key to abbreviations: isom.-isometric; tetr.-tetragonal; hex.-hexagonal; trig.-trigonal; G-specific gravity; F-fusibility; Cl-cleavage form; N-index of refraction; No-index of refraction for the ordinary ray; y-index of refraction for the intermediate ray; B-birefringence; ray; Mineral Chemical composition Pyroxene group: Aegirite. _.. (Na,Ca) (Mg, Diopside._._._. - Ca(Mg,Fe,Mn,Zn)8izO4- -.-.... Rhodonite. ..: Samarskite._...- (Y¥,Er,Ce,U,Ca,Fe,Pb,Th) (Cb, Steenstrupine... - (Ca,Na,Ce)s(OH)8izO1(?) ...--. Stilbite..~..... NaCa5(A111Si29) 030.30 Hzo _____ .~ Tilleyite _______ Cfis< 003)2Si207 _______________ Tourmaline... Na(Mg,Fe,Li)@Bs8isOx(OH):- -- . LitFe!' Ma") Le.: Uraninite...--. TUO;..? PENAL cll v Variscite._...... Wavellite...... ...--... Willemite._._.... 1 L I1 LULA SAY Sos Yttrotantalite.. - (Fe,Y,U,Ca)(Cb,Ta,Zr)041. __.. Hircon.....:... nuns Approzimate mazimum percent BeOQ 0.4 . O1 002 tr . OX . O1 O1 . O1 1. . 005 . 58 14(?) 2V-optic axial angle] Description Mono., long prism, vitreous; green; slightly soluble; Cl-110; H-6; G-3.5; F-2; N,-1.77-1.82; B-0.05; (-)2V-large. Mono., prismatic; vitreous; green; Cl-110; - H-5-6; G-38.2-3.3; E‘s—O5; N,-1.67;B-0.03; (+)2V- Tric., basal plates; vitreous; pink; CI-100, 010, 001; H-5.5-6.5; G-3.7; - F-4; _ N,-1,68-1.74; B-.01-.02; (+)2V-large. Orth., prismatic, tabular, massive; vitreous; black or brown; insolu- ble; Cl-O010; H-5-6; G-5.6-5.8; F-5; isotropic (from alteration); N-2.10-2.25; also strongly biref. (Unaltered) Hex., rhombohedral; dull; brown; H-4; G-3.3; uniaxial negative. Mono., tabular; pearly; white; de- composed by HCI; ClL-O10; H-4; G-2.1-2.2; F-2; N,-1.49; B- 011; (-)2V-830°%-50°. Tetr., prisms with pyramids; vitreous; brown; insoluble; Cl-110; H-5; (G-5.2-5.4; F-6; N,-1.8, com- monly isotropic from alteration, with N-1.7. Mono., colorless; CI-100, 101 (?); G-2.84; N,-1.63; B-0.04; (+) 2V-large. Trig., prismatic; vitreous; black, brown, green, red; insoluble; Cl- poor; H-7; G-2.9-3.2; F-4-6; N,-1.64-1.67; N,-1.62-1.64; B-0.02-0.03. Orth., prismatic; vitreous; greenish gray; soluble; CI-O001; 010, 110; H-5; G-3.4-8.6, _ F-1.5-2; N,-1.67-1.70; _ B-0.004-0.010; 2V-variable. Isom., octahedral, massive; submetal- lic; black; soluble in HNO;; H- 5.5; G-9; F-7. Orth., pyramidal or prismatic; green; soluble; Cl-O010; H-4; G-2.5- 2.9; F-7; N,-1.56-1.59; B- 0.02-0.03; 2V-variable. Orth., fibrous; pearly; white, green; soluble in HSO, and in NaOH; CI-110, 011, 010; H-4; G-2.3; F-7; N,-1.53; B-0.02-0.03; (+)2V-72°. Hex., prismatic; resinous; white, green, red; soluble; CI-0001, 1120; H-5.5; G-3.9-4.1; F-4; No- 1.70, N-1.72. Orth., prismatic; submetallic; black; insoluble; H-5; G-5.5-5.9; F- ;;1i530tropic from alteration, N- Tetr., prismatic; adamantine; brown; Cl-110 imperfect; H-7.5; G-4.7; N&-1.94, N.-1.98; B- 0.04-0.06. orth.-orthorhombic; mono.-monoclinic; trie.-triclinic; H-hardness Moh scale: N-index of refraction for the extraordinary Occurrence Syenitic rocks and related deposits; common. Pyrometasomatic, metamor- phic, and igneous rocks; very common. Ore deposits of manganese, iron, copper, generally with rhodochrosite. Granite pegmatite; rare. Syenitic pegmatite; rare. Cavities in basalt; common. Beryllian - variety (fore- site) in pegmatite; very rare. Pegmatite and syenite; rare. very Metamorphosed limestone, California; rare. Widely distributed in meta- morphic rocks, pegma- tites, and high tempera- ture veins; common. Granitic pegmatites; com- mon. Veins and granitic pegma- tites; rare. Sedimentary rocks. Secondary mineral in bedded ores; rare. Zinc deposits; uncommon. Granitic pegmatite; rare. Accessory mineral in igneous rocks, especially in gran- ite, syenite and diorite; common. - Beryllian vari- ety (alvite) in granitic pegmatites; very rare. 16 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES sions of beryllium minerals. The possibilities of the occurrence of beryllium in various minerals as a guest element, and the importance of these minerals as pos- sible sources of beryllium are discussed below. SULFIDES Beryllium is not likely to be precipated in sulfide lattices. However, it has been detected spectrograph- ically in gersdorflite, niccolite, and maucherite (Haw- ley, Lewis, and Wark, 1951, p. 154). The manner of occurrence of the beryllium is not known. Helvite and other beryllium-bearing minerals occur in sulfide de- posits, and minute inclusions of these minerals in the sulfides are a possibility. OXIDES In the Franklin district, New Jersey, beryllium was reportedly discovered in franklinite concentrates in 1944 (L. H. Bauer, written communication). Spectro- graphic analyses of carefully selected samples of franklinite taken at the Franklin and Sterling mills during the present investigation showed less than 0.0004 percent BeQ, the lower limit of sensitivity. Traces of beryllium have been detected in cassiterite from pegmatites and hydrothermal veins (Borovick and Gotman, 1939; Larionov and Tolmacev, 1937). The beryllium content of uraninite and other radio- active oxides was determined by Oftedal (1939) who found that most uraninite contains less than 0.01 per- cent beryllium. Most of the uraninite samples from the Colorado Plateau contain from 0.0001 to 0.0005 percent beryllium, however the uraninite from the Red Bluff area, Gila County, Ariz., contains as much as 0.005 percent beryllium (Thomas W. Stern, oral com- munication). The distribution of beryllium in the uraninite structure is not known. Bauxites containing as much as 0.018 percent beryl- lium and beryllium hydroxides readily form under similar conditions of surface temperatures and hydro- gen-ion concentrations. It is not known whether the small proportion of beryllium in the bauxite can be accommodated in the lattice of the finely crystalline, hydrous aluminum minerals or whether it forms dis- crete crystals of its own. An even more likely possi- bility is adsorption of the beryllium hydroxide to the surface of aluminum minerals. Detailed study of beryllium-rich bauxite might solve this problem. In general, the occurrence of beryllium in oxide minerals is unlikely because of structural difficulties and none may be regarded as a potential source of beryllium. HALIDES Fluorite samples from several veins contain as much as 0.00X percent BeO by spectrographic analysis, al- though none of the samples analyzed were from known beryllium mineral localities. The fact that fluorine does not favor tetrahedral coordination with beryllium suggests that beryllium in fluorite will be of small amount and restricted occurrence. However, the geo- logical occurrence of beryllium may be related to the presence of fluorine, as fluorite is a common constituent in many beryllium-bearing tactites, veins, and pegma- tites. CaARBONATES Although rhodochrosite from Kapnik, Hungary, and calcite from Franklin, N. J., are reported to contain traces of beryllium (Goldschmidt and Peters, 1932, p. 368), the difficulty of accommodation of beryllium in the lattice suggests that the maximum amount is extremely small. At Franklin, N. J., a district from which several beryllium minerals are known, only 1 of 10 samples of dolomitic marble contained more than the detectable minimum of 0.0005 percent BeOQ (L. H. Bauer, written communication). PHOSPHATES The substitution of beryllium for phosphorus is a possibility on the basis of comparable ionic size but ad- justment of valence is difficult. Although Nockolds and Mitchell (1948) and Goldschmidt and Peters (1932, p. 367) did not find beryllium in apatite from igneous rock, Schroeder (1931) found beryllium only in apa- tite, among all the rock minerals which he spectro- graphed qualitatively. Apatite from beryl-bearing pegmatite in the Newry and Rumford area, Maine, contained 0.002 percent BeQ. In the present investiga- tion one specimen of arsenian apatite (svabite) from Franklin, N. J., was found to contain 0.001 percent BeO; in three others it was absent. The principal mineral of phosphate rock is a member of the apatite family, but phosphate rock in the United States con- tains no more beryllium than the shale with which it occurs. Apparently apatite group minerals can con- tain only traces of beryllium. Wavellite, however, has been found to contain as much as 0.1 percent BeO (Preuss and Gliszezynski, 1951). NEOSILICATES In minerals of the garnet group a large number of trace elements have been detected, particularly the rare- earth metals, which enter by means of the substitution Y*AI* for Mn*Si* (Jaffe, 1951, p. 133). Beryllium MINERALOGY OF BERYLLIUM 17 has been detected in only a few varieties of garnet; typical examples are given in table 4. All known va- rieties of garnet containing appreciable beryllium are members of the grossularite-andradite series and are from pyrometatasomatic deposits. Helvite or other be- ryllium minerals occur in three of these deposits (Iron Mountain, N. Mex., Wykertown, N. J., Victorio Moun- tains, N. Mex.) and within a few miles of a fourth (Aarvold, Norway : Goldschmidt, 1911, p. 30) ; beryl- lium occurs in idocrase at all four. Samples from many of the garnet-rich pyrometasomatic deposits in the western United States were analyzed for beryllium in the present investigation ; of these more than 90 percent did not contain a detectable amount of BeO (0.0004 percent) ; the maximum content was only 0.002 percent BeQO. Many of these samples were nearly pure garnet. Beryllium was not detected in spessartite from beryl- and helvite-bearing pegamatites (Glass, 1985, p. 765). Apparently, no more than traces of beryllium can be expected in garnets except in helvite-bearing pyrometa- somatic deposits. TABLE 4.-Garnet analyzed for beryllia Composition Locality Percent BeO Reference Grossularite.__.. Iron 0. 08-0. 19 Glass and Mountain, others, N. Mex. 1944, p. 173. Andradite (And; - Wykertown, 0. OX-0. 0O0OX _ Milton and N.d: David- son, 1950, p. 504. Grossularite_.. .. Victorio 0. 007 Holser, Mountains, 1953, N. Mex. p. 603. Manganian Aarvold, 0. OOX _ Goldschmidt grossularite. Norway. and Peters, 1932, p. 369. Mill Creek, <0. OOOX () Mont. Grossularite__. _. Franklin, N. J. <0. 0004 (0) 1 Spectrographic analysis by A. A. Chodos. Spectrographic lines of beryllium were reported in willemite concentrate from Franklin, N. J. (L H. Bauer, written communication). In the present work, willemite was carefully picked from composite samples of average willemite concentrates. The material from Franklin, which is characteristically green, contained 0.004 percent BeQO ; material from Sterling Hill, which is characteristically pale red, contained 0.005 percent BeQ. No beryllium was detected spectrographically in willemite from Northern Rhodesia (L. H. Bauer, written communication). The structure of willemite is nearly identical to that of phenakite, zinc being in rare tetrahedral coordina- tion with oxygen (Bragg and Zachariasen, 1980). A small quantity of beryllium substitutes for zinc in this peculiar structure, despite the difference in ionic sizes. At the lower temperature at which supergene willemite forms by alteration of sphalerite (Pough, 1941, p. 98), the presence of beryllium in the solutions seems un- likely. Beryllium in willemite is apparently confined to that of high-temperature origin, as at Franklin, N. J. Idocrase contains beryllium more consistently than any other silicate in which beryllium is not an essential constituent, and of all such minerals that occur outside of pegmatites it contains the largest amount of beryl- lium (see table 5). 5.-Analyses of idocrase for beryllia BeO Locality (percent) Reported by- Franklin, N. J......:l.._, $:90..1... C. S. Hurlbut, written communication, 1951. Iron Mountain, N. Mex.. 1.09... Glassand others, 1944. Turnback Lake, North 107-°:.... Meen, 1939. West Territory, Canada. Victorio Mountains,. N. ..2....... Holser, 1953. ex. Graubunden, Switzerland _ .09---_-.-. Zilbermintz and Roschkova, 1933." Mill Creek area, Montana. - .OX-____- @). Aarvold, Norway _____--. OX. :f Goldschmidt and Peters, 1932. Breitenbrunn, Germany-. - Do. Julia mine, U. 8. S. R. (?). <.OL-_____ Zilbermintz and Roschkova, 1933. Johnson, :Ariz.._.:.... .L 005... _ _. (). Woodstock, Me.____.._._-- Present... (). Amherst, N. H.........~ (®). Carro de los Muertos, Small tr__. (@). Chihuahua, Mexico. Guffey, Cplo.:>........~.. None...... (3). Ternares mine, Durango, - None-__-. (). Mexico. 1 The several complete analyses of material from this locality are of an intergrown mixture of idocrase and diopside. 2 Spectrographic analysis by A. A. Chodos. 3 Spectrographic analysis by George Steiger. The structure of idocrase is similar to that of garnet and has been described by Warren and Modell (1931) and Machatschki (1930). A study of the distribution of beryllium in idocrase has shown that perhaps a third of beryllium in idocrase replaces silicon in tetrahedra, and the rest enters normally unoccupied tetrahedral posi- tions. Valence is balanced by loss of aluminum and some loss of calcium from the structure. Beryllian idocrase is consistently high in fluorine content, but there is no correlation with B, Ti, Zn, Mn, Cu, Na, K, or other minor constituents. With few exceptions idocrase is found only in allo- chemical metamorphic rocks (those which have received additions of material while being changed by heat and pressure). Within this general category, however, two general types of occurrence are common. In one, as exemplified by some of the occurrences in Switzerland and the Ural Mountains, idocrase is found at the con- tact of mafic intrusive rocks (usually serpentinized) 18 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES and limestone. A number of samples of this type of occurrence are among those of table 5 in which no beryllium was detected. - The second type of occurrence is in limestone near the contact of granitic rocks and is probably more common. All examples of idocrase con- taining 0.1 or more percent of BeQ are from the second type of occurrence (table 5). Several of these occur- rences are from localities at which helvite or other beryllium minerals have also been found, and at all such places fluorite is an associate of the idocrase. RING AND CHAIN SILICATES Tourmaline from pegmatites has been reported to contain as much as 0.0X percent BeO (Goldschmidt and Peters, 1932), but even that from beryl pegmatites commonly contains much less." Tourmaline from hypo- thermal veins has not been analyzed separately, but tourmaline-quartz vein material from the Lordsburg district, New Mexico, contained less than 0.0004 percent BeQO (table 14). Beryllium occurs in soda-rich pyroxenes and amphi- boles more commonly than in the normal members of these groups. Goldschmidt and Peters (1932, p. 366) reported 0.1 percent BeQ in aegirite, and 0.X percent in arfvedsonite and barkevikite. One sample of aegirite from Wind Mountain, N. Mex., contained only 0.000X percent BeO. The foregoing are all from pegmatitic facies of nepheline syenite intrusive rocks, but zincian- manganoan diopside from Franklin, N. J., was found also to contain 0.01 and diopside-hedenbergite from Mill Creek, Mont., contained 0.00X percent BeQ. Goldschmidt and Peters (1932, p. 367) list two am- phiboles of metasomatic origin containing 0.00X per- cent BeO and one enstatite in which beryllium was not detected. An augite which contained less than 0.001 percent BeO was from basalt, and a pyroxene in which beryllium was not detected was from eclogite. Nock- olds and Mitchell (1948) analyzed the hornblendes and pyroxenes from a series of Scottish igneous rocks rang- ing nearly continuously in composition from dunite through granodiorite. One hornblende sample con- tained a questionable 0.003 percent BeQ, which was the limit of sensitivity, and the rest showed no BeQO. Bray (1942b, p. 794) did not detect any beryllium in five samples of hornblende from granodiorite. In syn- thetic fluo-amphiboles, beryllium has been substituted for silicon to the extent of 12 percent of the tetrahedral groups (about 3 percent BeQ) in both lime- and soda- rich varieties (Comeforo, Hatch, and Eitel, 1950). The presence of beryllium in pyroxenes and amphiboles is probably due largely to beryllium concentration dur- % Average of 0.006 percent BeO in blue, green and pink tourmaline from the Newry and Rumford area, Maine; analyses by J. D. Fletcher. ing differentiation of sodium-rich magmas, from which these minerals are late to crystallize. Rhodonite is associated with beryllium minerals at several places, including Franklin, N. J., Butte, Mont., and the Sunnyside mine, near Eureka, Colo. An analy- sis of rhodonite from Franklin, shows 0.002 percent of BeO. Samples of vein material in which rhodonite is the principal gangue were taken from the Butte dis- trict during the present study. The BeQ content in these samples ranged from 0.0005 to 0.007, and in most of the samples helvite was observed. Samples from the Sunnyside mine showed little helvite and contained an average of less than 0.001 percent of BeQ. One sample from Bill Young mine contained 0.0016 per- cent BeO; no helvite was identified. Beryllium was not detected in samples of other rhodonite veins at localities in the San Juan region, Colorado, from which no beryllium minerals have been reported. Manganese-bearing members of the epidote group have been reported to contain traces of beryllium (Glass and others, 1944, p. 177). The ordinary pistacite variety has not been analyzed separately for beryllium, but a large number of epidote-rich tactites analyzed in the present investigation contain a maximum of 0.0008 percent BeQ (table 15), but in 75 percent of them BeO was below the limit of detection. Allanite, which is structurally and chemically related to the epidote group, is reported to contain as much as 5.52 percent BeOQ (Dana, 1892, p. 526). All allanites con- taining more than 0.5 percent BeQ were highly altered and all were from pegmatites. Beryllium was not de- tected in the unaltered allanite of hydrothermal origin at Wykertown, N. H. (Milton and Davidson, 1950, p. 504). SHEET SILICATES Complex substitutions of various ions in sheet silicates are common, and opportunities for the occurrence of beryllium are numerous. Micas from pegmatites have been found to contain a maximum of 0.0X percent BeQO (Goldschmidt and Peters, 1932, p. 366), but no beryl- lium was found in micas from a series of igneous rocks (Nockolds and Mitchell, 1948, p. 564-565). Fluorine- phlogopite has been synthesized as much as one-fourth of the silicon being replaced by beryllium (that is, K,Mg,BeSi;OmF,=about 3 percent BeOQ) (Eitel, Hatch, and Humphrey, 1950). This is an example of replacement of Al"Al" by Be#*Si* in tetrahedral coor- dination, a process which may be important in other alumino-silicates. Another replacement observed was AlAl by BaBe. Such replacements in synthetic flu- orine-muscovite are more restricted. Data on natural micas do not yet indicate any preference of beryllium MINERALOGY OF BERYLLIUM 19 for those of a particular mode of occurrence or of a par- ticular composition. A large number of representative samples of clay minerals were analyzed spectographically for beryllium by Wheeler and Burkhardt (1950). All of the mont- morillonites that originated through surface or sub- marine alteration of tuffaceous rocks were found to contain beryllium, the maximum content being 0.01 percent BeQ. Beryllium was found in nearly all of the kaolinite-group samples that were of hydrothermal ori- gin (maximum 0.008 percent BeQ), but could not be detected in most of those of residual origin. Illite formed by soil alteration contained a maximum of 0.008 percent BeQ. None was detected in attapulgite. None of these clays appear directly related to bauxite de- posits formed by alteration of syenitic igneous rocks. Szelenyi (1937) reported that some clays contain about the same amount of beryllium as the associated bauxite (0.005 to 0.01 percent BeQ), although others contain less. In addition to the mechanisms proposed above for other silicates, a new interpretation of the mont- morillonite structure (McConnell, 1950) suggests the further possibility of replacing by BeSisH»O010 in the tetrahedra. Chlorite (Glass and others, 1944, p. 177), pyrophyl- lite (Wheeler and Burkhardt, 1950, p. 80), and apoph- yllite (Goldschmidt and Peters, 1932, p. 867) have been reported to contain small amounts of beryllium. FRAMEWORK SILICATES Beryllium is found in small quantities in feldspars (table 6). Although the maximum beryllium content recorded for albite is higher than that for the potassium feld- spars, a few determinations show the averages not to be significantly different. The alkali feldspars as a group contrast markedly with calcic plagioclase, in which beryllium has not been detected. - Nockolds and Mitchell (1948) tested 11 potsassium feldspar samples and 9 plagioclase samples from a variety of igneous rocks; all contained less than 0.003 percent of BeQ, the limit of sensitivity. Bray (1942b, p. 790) was not able to detect beryllium spectrographically in 17 samples of feldspar from either pegmatites or related igneous rocks near Jamestown, Colo. Substitution of beryllium in feldspars is stable when the beryllium is in tetrahedral positions in place of silicon or aluminum (Schiebold, 1981). Available data on nepheline (Tolmacey and Filippov, 1934; Goldschmidt and Peters, 1932, p. 366) indicate that beryllium may have about the same solubility in the nepheline lattice as in that of the alkali feldspar. However, nepheline seems to have a higher average beryllium content than feldspar minerals. Most of the analyzed nepheline and feldspar minerals are from peg- matites. A lower beryllium content for these minerals in finer grained intrusive rocks may be surmised from spectrographic analyses of igneous rocks. Feldspath- oids other than nepheline have not been analyzed for beryllium. Analytical data for the amphiboles, micas, feldspars, and feldspathoids show approximately the same maxi- mum beryllium content for each, this suggests that be- ryllium substitution is controlled by a feature common to these minerals. This common feature is the presence of four-coordinated aluminum, permitting the substi- tution of BeSi for AlAl. Silicates of this type, in- cluding all the framework silicates except quartz, all the sheet silicates, and hornblende in the chain silicate group, should have comparable solid solubilities for beryllium. Therefore, when formed in environments of similar beryllium concentration, these minerals Tasur 6.-Beryllia content of 14 samples of feldspar BeO kie. ock ais bers. Reference Microcline _ Granite pegmatite____.. Risey, Norway. _..__L_..cozz <0. O00 X Golggchmidt and - Peters; 1932, p. 366. yo! au: ganic le: i golt:. "" ss o Pikes Peak, Colo: . 00x Do. is lls: s Pegmatite(?): ..o. cu .jel UcoBaS. ey. . 04 Filippov and Tolmacey, 1935. Boda microcline_.___......- Syenite pegmatite... Langesundfiord, Norway... . OO X Goldschmiit and - Peters, 1932, p. 366. {s LGo.. soles .-- tous as Laven, . OO X Do. Perthite zone, granite Ridge pegmatite, Red Hill, . 003 (!) pegmatite. Maine. on ani =o: a . 003 (1) Granite pegmatite... Rumford, Maine_...._...... . 003 (1) Albfte.. "2... 22s. Mill Creek, . OX ) Granite pegmatite... Newry and Rumford, Maine. . 002 (4) ich -r 8 - -a afle . =s ann ess . 006 (!) Derix NOL L iC do Y.-L. AAs Kragero, Norway.____..1:LL . O1 Goldschmidt _ and - Peters, 1932, p. 366. Labradorite.........>:r,. Anorthogite-.'.=,.=<-<- Sogon, Nortway..~...-...-.-.- <. O0 X Do. Bytowniltes......_.lL:.;.« iro MO.. bets ££ 310d0....: . sta en- tp <.. O00 X Do. 1 Spectrographic analysis by J. 2 Spectrographic analysis by A. Chodos. Ii. Fletcher; specimens collected by V. E. Shainin. 20 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES should contain comparable quantities of beryllium. However, a wide range is to be expected, owing to the variety of geologic environments in which the minerals crystallize. BERYLLIUM IN IGNEOUS ROCKS UNITED STATES LOCALITIES The few data on the beryllium content of igneous rocks in the United States are summarized in table 7. Some of these analyses, originally stated in terms of percent beryllium, were converted to percent BeQ in order to facilitate comparisons with results of the present investigation. Most of the original analyses were stated to only one significant figure; consequently, the converted result gives an impression of greater accuracy than was intended by the analyst. Besides the semiquantitative determinations listed in table 7, many qualitative determinations have been made most with negative results. Spectrographic tests of a representative suite of igneous rocks from the Spanish Peaks region, Colorado, showed negative re- sults for beryllium, but the limit of detection was about 0.02 percent Be (Knopf, 1936, p. 1779). Spectrographic analyses of 425 miscellaneous rocks and ores were tabu- lated by Freeman (1942, p. 777, 778) and only one, a weathered granite, contained more than the detectable limit of 0.001 percent Be. Bray (1942a, p. 431; 1942b, p. 784, '(85) reported qualitative spectrographic analyses. of 19 samples of Precambrian granites, 9 samples of Tertiary granodiorite, and 7 samples of Tertiary quartz monzonite, all from Colorado, and 9 samples of granite and 2 of granodiorite from Massachusetts. None showed beryllium, but the sensitivity of the tests is not stated. Tapu® 7.-Beryllia content of igneous rocks of the United States, as published BeO S102 Rock Locality (percent) (percent) Reference ._ iet Yellowstone Park, Wyo. _._______. 0. O1 75 Goldschmidt and Peters, 1932, p. 365. Nepheline syenite_____________ Magnet Cove. Ark. ... . OOX 49. 7 Do. Granite "i Babyhead, Llano County, Tex. . 004 75. 20 Sandell and Goldich, 1943, p. 169. Granite l." Oraniteville, Mo. . 003 76. 81 Do. . Berti? Mountain, Gillespie County, . 003 76. T7 Do. ex. Granite.... :l t ul Granite Mountain, Burnet County, . 002 73. 02 Do. Tex. _ :. 10 ___ is Defifi Track River, Cook County, . 002 73. 6 Do. inn. . >---. sees cee ce eol a Cassaday quarry, Llano County, . O01 72. 15 Do. Tex. Albite-nepheline syenite. _ Titchfield, . O01 60. 39 Goldschmidt and Peters, 1932, p. 365. Quartz To’Fn Mountain, Llano County, 0008 68. 15 Sandell and Goldich, 1943, p. 169. ex. Granitic rock@4....0_ -o: oli-. Minnesota _ 0008 : Do. -- cri Malmo, Aitkin County, Minn... 0006 71. 19 Do. Null 0005 52. 70 Sandell, 1949, p. 91. ece Do -Ri_.L .C: . 0003 46. 88 Do. Quartz _. Paedad; <. 0004 64. 49 Anderson, 1950a, p. 617-18. ._ [LIL "N] __ " Jackson Connty, N. C._.._.._.._____ 000x ' Goldschmidt and Peters, 1932, p. 363. 1 Composite of five samples. Many igneous rocks in the United States were ana- lyzed spectrographically for beryllium (table 8). Though a variety of rock types was included in the present sampling, particular attention was paid to silicic and alkalic intrusive rocks, for experience of previous workers appeared to indicate that these are most likely to contain beryllium. The composite alkalic intrusive rocks at Iron Hill, Colo., northeastern New Mexico, Magnet Cove, Ark., and in Trans-Pecos Texas, were sampled extensively and account for the many rare and uncommon rock types included in the table. With the exception of granite, less emphasis was directed to the more common igneous rocks of the Western States. Gra- nodiorite and other intermediate types are poorly rep- resented. The lower limit of beryllium determination for some samples was as high as 0.004 percent BeQ but for most samples it was 0.001 percent BeQ or less. The table in- dicates that those rocks that contain more than 0.001 percent BeO are mainly of silicic or alkalic varieties, whereas those of less than this amount are for the most part the more mafic types. Notable exceptions to this generalization occur in the Iron Hill rocks, where un- compaghrite (melilite-diopside rock) and pyroxenite, which are low in silica and alkalis, contain most of the beryllium, whereas nepheline syenite and soda syenite show abnormally low beryllium content. FOREIGN LOCALITIES Spectrographic analyses of many igneous rocks from localities outside the United States are included in the reports of Goldschmidt and Peters (1932), Rodolico (1943), Rodolico and Pieruccini (1943), Wager and Mitchell (1948), Sahama (1945a ; 1945b), and Nockolds and Mitchell (1948). Beryllium was among the minor elements determined or looked for in many of the sam- ples. Data flor these samples and for a few others from BERYLLIUM IN IGNEOUS ROCKS TaBu® 8.-Beryllia content of igneous rocks of the United States, as analyzed for this study 21 miscellaneous foreign sources are summarized in table 9. The results compare favorably with those obtained for igneous rocks in the United States (table 8). Number Percent BeO Rock Form Locality Associated of metals analyses ! High Low Average Feldspathoidal: Melanocratic: Nepheline pyroxenite........~ Tron Hill, Gunnison County, Colo..._.___..._....- None.-_.....«< $ {.A. Pera <0. 001 Analcite gabbro.............- Huerfano Butte, Huerfano County, Colo..._____._|..... 1 2.002 Shonkinite. .... i Magnet Cove, Hot Springs County, Ark.. ves 1 <. 001 Gordon Butte, Meagher County, Mont... 1 <. 0001 -..: .. Leucite Hills, Sweetwater County, do:....s., 1 <. 001 Malignite (some nepheline- Wind Mtn., Otero County, N. Mex.....____.__.~ BAA 10 0. 03 0. 001 .016 syenite pegmatite). Leucocratic: Nepheline syenite...........- Analcite-nepheline syenite...... Nepheline-sodalite syenite.... Nepheline syenite pegmatite (see also malignite). Albite Granite porphyry .. Rhyolite porphyry....... Rhyolite breccia See footnotes at end of table. Dike..........+s Plug(?)=....:c.- Laccolith_...... -| Leucite Hills, Sweetwater County, Wyo..._...... Leucite syenite porphyry. Phonolife............ Do... Do... Orendite.. .. Uncompaghrite..........__.. Do. (altered)-............ Syenitic: Porphyritic syenite......._____... Plug:... ..- Do.... 22.0900 etl. als Sills. Mp... l.. sc lal coll dene Plug... [reek A0. SyBNIG-.zs 0222.00 -e ues Ring dike(?) ...- DQceer ect io leon aon cedega Plugs... DOL: . Dol Rell: lice cn ine Ring dike(?) ...- Soda syenite.. Dike..... 000.0 uue -...... Granitic: CTRRINGL OE: C-- 22000 bau dune k. a Batholith... {no Magnet Cove, Hot Springs County, Ark..._...... Little Rock, Pulaski County, Ark.... Bauxite. Saline County, Wind Mtn., Otero County, N. Mex..__..____.... _____ 00. .. Black Mtn., Otero County, N. Mex__.___._.__..- Wykertown, Sussex County, N. J..._.______.______ Sussex, Sussex County, N. J...... Beemerville, Sussex County, N. J._..______.____.- Little Wind Mtn., Otero County, N. Mex._....~ Red Hill, Carroll County, N. H...... Wind Mtn., Otero County, N. Mex..._.__.._._.~ Little Rock, Pulaski County, Ark.______._____.___ Magnet Cove, Hot Springs County, Ark._.......~ Chico, Colfex County,. N. Mex......._:.........s. Bryant, Saline County, Ark.... Annie Creek, Lawrence County, S. Dak__.___._._ Tron Hill, Gunnison County, Colo... _____ 10: L ae as Magnet Cove, Hot Springs County, Ark.___._..._ Tron Hill, Gunnison County, Colo.... ..... . =~ -z-oude cock sae sens sea ene an Magnet Cove, Hot Springs County, Ark._._...... Leucite Hills, Sweetwater County, Wyo.......... Cornuda Mtn., Otero County, N. Mex.._........ Dog Mtn., Hudspeth County, Tex....___....__... Cerro Diablo, Hudspeth County, Tex...__.._..... Hueco Tanks, El Paso County, Tex._....__.._.. Cerro Alto, El Paso County, Tex......_____._._... Wylie Mts., Culberson County, Tex.___________.. San Pedro Mts., Santa Fe County, N. Mex.. Ortiz Mts., Santa Fe County, N. Mex._....___... Red Hill, Carroll County, N. H....._......_..... Tron Hill, Gunnison County, Colo...............~ Chico, Colfax County, N. Mex...____.__.___.___.. PAIGE N. .... L IDL CORE ece s Tron Mtn., Albany County, Wyo.... Harney Peak, Pennington County, S. Dak._..... Star mine, Harrison Pass, Elko County, Nev Rose Creek mine, Pershing County, Nev...__...~ Nevada Scheelite mine, Mineral County, Nev.... Round Valley mine, Tungsten Hills, Calif... Rocky Canyon, Humboldt Range, Nev.. Sheeprock Mts., Tooele County, Utah... Limerick Canyon, Humboldt Range, Nev. Victorio Mts., Luna County, N. Mex.... Cave Peak, Culberson County, Tex...___._____... ..... AL LL conn coe ense 22 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 8.-Beryllia content of igneous rocks of the United States, as analyzed for this study-Continued Rock Form Locality Number Percent BeO Associated of metals analyses ! High Average Granitic-Continued Aplite (altered)... Aplite-pegmatite. .... Aplitic granite........ Intermediate: Granodiorite. ...... San Antonio Mt., Sandoval County, N. Mex.... ..... OOo arcane risen abr as Star mine, Harrison Pass, Elko County, Nev.... Limerick Canyon, Humboldt Range, Nev.. Oreana area, Humboldt Range, Nev............... Round Valley mine, Inyo County, Calif...... Nevada-Massachusetts Co. mine, Pershing County, Nev. Rocky Canyon, Humboldt Range, Nev......._... Aeroplane mine, Tungsten Hills, Calif....___..___ Santa Rita, Grant County, N. Mex...._._____.__. Nevada-Massachusetts Co. mine, Pershing County, Nev. Ragged Top mine, Pershing County, Victory mine, near Gabbs, Hanover, Grant County, N. Mex.....__._______.. Sheeprock Mts., Tooele County, Utah_..__._..... j ws... s Zn, Cu, Pb... Anortho8ite. . . .- 1. 02.0, . uue oue Iron Mtn., Albany County, Wyo....._.______..... Mafic: 00000... 0% Dike -..] Sandus, Sanders County, Mont._..______________. .eu son s do. : zea Tron Mtn., Albany County, Wyo...__....._.____. DiADASG. O. repo lloc els buss Morley, Las Animas County, Colo. Posslt..-z.-..._ Chico, Colfax County, N. Mex...__.. Pyroxenite....... * Iron Hill, Gunnison County, Colo... Biotite pyroxenite..._.__...._._._|..... [tls poon ome ou (3 10 lot comment retain o commin ne, ul Lamprophyre. 2. Fort Washakie, Fremont County, Wyo... . Shonn renee lae Snowmass Mtn., Pitkin County, Colo..___.._._.. Little Dragoon Mts., Cochise County, Ariz.. Panther Canyon, Humboldt Range, Nev.... Acroplane mine, Tungsten Hills, Calif.._._._.___... Union mine, Atolia district, Calif.... Pine Creek mine, Inyo County, Calif.... Aeroplane mine, Tungsten Hills, Calif... Little Sister mine, Inyo County, Calif.... Paliza Canyon, Sandoval County, N. Mex. W, Cu, Zn.... * Unless otherwise noted, all analyses are of samples collected during this investi- gation. 2 Determined on plates exposed for general scanning, and not for precise determina- tion of BeO. 3 Material collected by Mackenzie Gordon, U. S. Geological Survey. + Composite. 5 Material collected by A. S. Wilkerson, New Jersey Bureau of Mineral Research. ® Material collected by Fred Hildebrand, University of Chicago. DISTRIBUTION OF BERYLLIUM IN IGNEOUS ROCKS The average BeQ content of various types of igneous rock is important to a basic understanding of beryllium geochemistry. Furthermore, this information may in- dicate what kinds of rock are favorable for beryllium prospecting, and what amounts may be considered sig- nificant in a given rock type. Goldschmidt and Peters (1932, p. 370) made the first detailed estimate of the content of beryllium in igneous rocks, as follows : BeOQ Rock type (percent) Average igneous rock 0.0005 Nepheline syenite 01 Granite a 001 Gabbro ©0003 *+ Added later (Goldschmidt, Hauptmann, and Peters, 1933, p. 364). ? Material collected by the Mine, Mill, and Smelter Survey, U. S. Geological Survey. 8 Material collected by D. M. Henderson, University of Illinois. ° Material collected by J. W. Adams, U. S. Geological Survey. * Material collected by J. J. Norton, U. S. Geological Survey. ! Material collected by C. S. Ross, U. S. Geological Survey. " Material collected by J. R. Cooper, U. S. Geological Survey. Since then other estimates have been made, somewhat increasing the amounts for both granite and average igneous rock and substantially reducing the figure for feldspathoidal rocks. However, recent estimates by Sandell (1952, p. 212-213), based on fluorimetric deter- minations of beryllium in composite samples of igneous rocks from various localities, agree essentially with the values given by Goldschmidt and Peters for granite, gabbro, and average igneous rock. The analyses by Goldschmidt are not strictly compa- rable with those of some later analysts because his are given only in powers of ten, although the figures given by others may not be precise. On the other hand, the greater accuracy of the more recent determinations has been offset by discovery of a wider range in beryl- BERYLLIUM IN IGNEOUS ROCKS 28 9.-Beryllia content of igneous rocks from foreign localities Number of Rock Locality samples High Low Average Reported by- FELDSPATHOIDAL Melanocratic types._____ Portugal=:............. 2 ~ 0. OX 0. OOX O. O1 Goldschmidt and Peters (1932). Doélal:- Cuil t_ Fennoscandia_._-______ A at f s _L <. O01 Do. Leucocratic types...... Til Peers 1 enas . OX Do. 2 . O1 . O01 . 005 Do. Do. c... earl 7. . O1 <. O01 . 003 Do. Zilbermintz and Roschkova (1933). Do....s. 2 il as ffunsafy...:......l..... 2 . 001 001 . 001 _ Goldschmidt and Peters (1932). :l 2 iv} 2 . OOX . OOX . OOX Do. Dore r ei seee ue Southern Russia________ PB serier ial e c 22s <. O1 Zilbermintz and Roschkova (1933). 2 -<. 001 <. O01 <.. 001 _ Goldschmidt and Peters (1932). Mixturen: 1 sy. 3:0. 30°_ World 2. c: uct +29 . oc "us Ges . 001 _ Goldschmidt and Peters (1983). SYENITIC Syenite= s Fennoscandia....._._... 1; ; wile a ~ 0. 001 _ Goldschmidt and Peters (1932). Dols 222.180.0100 _- -do Pt s 11 £109." [ URL] 7 . 0006 Sahama (19452). Trachyte-==>. -t. . >eu MalyL FELL : .s. 2 0. 0030 0. 0022 . 0026 Rodolico and Pieruccini (1943). GRANITIC Ifaly. [. 400 ." ance 2 0. 0033 0. 0021 0. 0027 Pieruccini (1943). Moilk: li. _Miliuil Germany...... ADEL Lares" rina = aand . 002 _ Goldschmidt and Peters (1982). MALY -. an- 2 s 2 0018 . 00046 . 0011 Pieruccini (1948). sella 21 Germany.: ~" _i" 5 O0X _ <. 001 . 001 _ Goldschmidt and Peters (1932). ., Fennoscandia._._--__.___. O1. L i XL . 001 Sahama (1945b). Doss as. e4U0- P- 4. ie c= 2 . OOX . OOL . O0OX - Goldschmidt and Peters (1982). Doss caa sen nent ...s 1 42 . 0003 . 00083 . 0003 Sahama (1945b). Seotland of. ib it'" {run" Si <. OOL <. 001 <. 001 __ Nockolds and Mitchell (1948). Fennoscandia... 5 . 0003 <.0003 <.0003 Sahama (1945b). Granophyre......:..._.. Greenland.. 2 <. 008 <. 003 <. 003 _ Wager and Mitchell (1943). Reotland:......._>>. . I _ c, <. 001 _ Nockolds and Mitchell (1948). Obsidian... .... jaw.... 3 . O01 . O01 . 001 _ Goldschmidt and Peters (1982). Granodiorite and 9 <. 001 <. O01 <. 001 _ Nockolds and Mitchell (1948). adamellite. fTondlites............. Germany-Fennoscandia . 3 . O01 <. O01 <. 001 - Goldschmidt and Peters (1932). Do: Seotlaud: :? $014. __ e -P GPL <. 001 _ Nockolds and Mitchell (1948). MAFIC {AIF Ane. Ae url unl . raitt oke a cen s 0. 0011 Pieruccini (1943). _______________ Peotland-s =i: _ MOull 9 <0. 001 <0. O01 <. 001 _ Nockolds and Mitchell (1948). .c o .. HME! /. ct eca {Mic Ho 1 . . 0003 Goldschmidt and others (1933). 1220.4: -ne veal O@reenland:..:..22..2. 7. '<. 003 <. 003 <.003 _ Zilbermintz and Roschkova (1933). Doss ri t i-. Scotland """ !t [XTL °° 6 <. 001 <. O01 <. 001 _ Nockolds and Mitchell (1948). Dour! Fennoscandia... 1124 001 . L 5 yore A [ as <. 0001 - Sahama (19452). ermany.--..>>=...~... 8 <. 001 <. O01 <. 001 _ Goldschmidt and Peters (1932). l_ e- icf "Lf _ goh t T_ . gos <. O01 Do. Peridotite:s: .L Reotland sc. 2 . <. 004 <. 001 <. 001 _ Nockolds and Mitchell (1948). ~ -MD -s rales apne 1. 0 - .s <. 001 Do. "Ultrabasics"_"l___:!. Fennoscandia. s} le Sill aln l NL BTO <.. 0001 Sahama (19459). 1 Mixture. lium content for a given rock than was previously ex- pected. An attempt has been made to adjust the aver- age BeO contents for igneous rock types to fit the data obtained in the present investigation; the following values are suggested : BeQ Rock type (percent) Average igneous rock 0.001 Feldspathoidal rocks 0025 Granitic rocks 002 Syenitic rocks 001 Intermediate rocks 0007 Mafic and ultramafic rocks 0001 The present study has provided much information concerning the presence of beryllium in alkalic intru- sive rocks in the United States, as most of these were BeO content, in percent sampled in detail. The average value of 0.01 percent BeO given originally by Goldschmidt and Peters for nepheline syenite seems much too high, as the only analyses in their data that exceeded the figure were the very extraordinary "sodalite-eudialyte rock" (alkalic syenite) and "pedrosite" (alkalic hornblendite). Their revised figure of 0.003 percent BeOQ (Goldschmidt, Hauptmann, and Peters, 1933, p. 864) is close to that proposed by us. The analytical data of Goldschmidt and Peters on rocks from Magnet Cove, Ark., compare favorably with our results. (See tables 7 and 8.) They report 0.004 percent BeQ in nepheline syenite from that locality, whereas the present investigation disclosed a maximum of 0.002 percent BeQ and an average of about 0.001 percent. 24 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES The average beryllium content of feldspathoidal rocks gives little weight to the less abundant mafic vari- eties. However, the average beryllium content of the mafic varieties probably exceeds the total average by as much as 0.001 percent BeQ. At Iron Hill, Colo., Wind Mountain, N. Mex., and Alter-Pedrosa, Portugal, the highest contents were all in pyroxene- or amphibole- rich rocks, but in southern Norway the highest was in laurdalite, a type of nepheline syenite commonly poor in minerals of the pyroxene and amphibole groups. In comparing the chemical analyses and modes so far available, no consistent correlation between beryllium content and mineralogy is apparent. The tendency for higher BeQ content in the mafic types may be attrib- uted to the admittance of larger amounts of beryllium into the lattice of aegirite than into other minerals of feldspathoidal rocks (see table 3) and to the tendency for pyroxene and amphiboles to crystallize last in many alkalic intrusive bodies (Fersman, 1929, p. 22-27). The granites analyzed in connection with the present investigation (see table 8) average somewhat higher in beryllium content than those of Goldschmidt and Peters (table 9) or Sandell and Goldich (table 7), being about 0.004 percent BeQO. - However, many of the samples probably are not representative : those from Sheeprock Mountains, Utah, and Mount Antero, Colo., are from areas known to be rich in beryl, and others are from small granitic intrusive bodies in metal-mining districts of the western United States. Although such rocks probably do not contribute greatly to the world average for granitic rocks, they should serve to raise the beryllium content somewhat above the minimal values obtained for other granites. The value of 3 ppm beryllium (about 0.0008 percent BeO) suggested by Sandell (195%, p. 212) for the average granite thus may be too low, and the 0.002 percent BeQO suggested by Goldschmidt, Hauptmann, and Peters (1983, p. 364) is taken as a suitable compromise for the present. Re- sults of our analyses seem to indicate that granitic rocks associated with major ore deposits have higher than average beryllium content. Nonfeldspathoidal syenites appear to contain less beryllium than granites, although they have not been sampled extensively. Quantitative data on granodiorites are lacking. The new analyses contribute little to the knowledge of beryllium content of the more mafic rocks, except to confirm that they most commonly contain less than 0.001 percent BeQ. The only high value was obtained from a pyroxenite associated with the alkalic intrusive at Iron Hill, Colo. The average value given is that of Goldschmidt, modified by the determinations of Sahama. Analyses of extrusive rocks are few, but those avail- able do not differ noticeably in BeO content from the average for the corresponding intrusive rocks. The beryllia content of the average igneous rock was calculated by the method of Knopf (1916, p. 620) and, like the figures on which it is based, must be considered as tentative. The value of 0.001 percent BeO thus obtained is intermediate with respect to averages rang- ing from 0.0005 to 0.002 percent BeO given by others (Goldschmidt and Peters, 1932, p. 371; Noddack and Noddack, 1934, p. 173; Sandell and Goldich, 1948, p. 181; Sandell, 1952, p. 218). In comparing the new averages for the various rock types with that of the average igneous rock, the writers confirmed their earlier conclusion that beryllium is con- centrated in granites and feldspathoidal rock, but the difference in average BeO content for granite and feldspathoidal rocks is much less than formerly sup- posed. The formation of granite and feldspathoidal rocks is attended by a concentration of alkalies and volatile components, and apparently beryllium tends to be concentrated in the process. In feldspathoidal rock the process of differentiation apparently is such that beryllium tends to be concentrated in the more mafic facies. MODE OF OCCURRENCE At most localities where beryllium has been detected in igneous rocks the beryllium-bearing mineral or min- erals have not been determined. 'The occurrence of beryl and phenakite as miarolitic fillings, schlieren, segregations, and individual grains in granite at Mount Antero, Colo., and in the Sheeprock Mountains, Utah, suggest that these minerals may be present in other beryllium-bearing granites. Microscopic beryl in granite was described by Hartley (1902, p. 285). The theoretical upper limits for BeQ content in igneous rocks containing no beryllium minerals (that is, beryl, helvite, etc.) may be approximated by total- ling the maxima (see table 3) for the various mineral species in the rock. For an average granite this would be about 0.02 percent BeQ, with mica as the principal carrier. However, most of the analyzed rock minerals are of specimens from pegmatites and are therefore most likely to be saturated with beryllium, but also are more likely to contain inclusions of beryl and other beryllium minerals The grade of beryl ore in pegmatite zones (Hanley and others, 1950, p. 11) sug- gests that the average BeQO content of most pegmatites does not greatly exceed 0.02 percent, or that of an average granite. Possibly the beryllium in some gran- ites containing this amount of BeOQ may be present in part as minute crystals of beryl or phenakite. In feldspathoidal rocks beryllium may be present as BERYLLIUM IN SEDIMENTARY ROCKS 20 an accessory constituent in minerals, mainly in aegirite. Goldschmidt and Peters (1932, p. 366) give the follow- ing analytical data on minerals from a nepheline-sye- nite pegmatite at Laven, Langesundsfiord, Norway : BeO Mineral (percent) Aegirite____- 0.1 Nepheline . OX Soda-microcline . OOX Lepidomelane . OOX The theoretical maximum beryllium content for an average nepheline syenite is approximately 0.04 per- cent BeQ. Even in the pegmatitic phase of these rocks, beryllium minerals are rare. Furthermore, pegmatite is not so common in feldspathoidal rocks as in granitic rocks. Detailed analytical work on the feldspathoidal rocks from Wind Mountain, N. Mex., indicates that all the beryllium is present in rock minerals, and that it is nearly as abundant in the parent rock as in pegma- tite. The highest contents were found in the malignite (aegirite-rich) facies of the pegmatitic rocks and in the aegirite-rich hornfels associated with it. BERYLLIUM IN SEDIMENTARY ROCKS CLASTIC DEPOSITS The concentration of beryllium in clastic sedimen- tary rocks depends largely upon the effect of weathering on the beryllium-bearing minerals and the extent to which gravity may have concentrated these minerals. The weathering of beryllium minerals has not been studied as such, but some information was obtained on chemical weathering of beryllium minerals through study of hydrothermally altered beryl and danalite. Altered beryl from pegmatitee in Brazil (Kerr, 1946b) and Korea (Iwase and Ukai, 1944) shows an increase in water and a decrease in silica, alkalies, and specific gravity. In these and other studies of altered beryl, the effect of alteration on beryllium content is not certain. Generally some beryllium is lost, although in the Korean material a slight gain perhaps due to secondary bertrandite was noted. Some investigators are of the opinion that the water in beryl analyses is due to included alteration products (Caglioti and Zambonini, 1928 ; Folinsbee, 1941, p. 488). However, the fact that beryl loses water slowly and ir- reversibly at 800°C (Allen and Clement, 1908, p. 115 116) indicates that the water is probably held in the beryl structure rather than in the structure of an alter- ation product. According to Kerr (1946b, p. 436) and Waldschmidt and Adams (1942, p. 34), kaolinite and muscovite are products of highly altered beryl. At temperatures as high as 800°C, beryl was stable in 467945-59--8 laboratory experiments that largely decomposed feld- spars and many other silicates (Norton, 1939, p. 11). Danalite has been found altered to phenakite, side- rite, sphalerite, and pyrite (Palache, 1907, p. 252-254), but no other alterations of the helvite group minerals have been recorded. Aside from the rare presence of bertrandite, reten- tion of beryllium in the alteration product is uncertain. Although Kerr's analysis of the kaolinite-rich product showed 0.24 percent BeQO, he assumed in his calculations that this was owing to contamination by beryl (1946b, p. 439-440). Probably most beryllium minerals do not weather chemically except under extraordinary circum- stances. Many of the silicate minerals in which beryl- lium is a minor constituent, such as feldspar, nepheline, and micas, decompose easily under surface conditions. The decomposition involves an intermediate dissolved state (Correns and Engelhardt, 1938) in which there is a breakdown of the oxygen tetrahedra, accompanied by the release of colloidal silica and beryllium. The specific gravity of most beryllium minerals, which is 2.6 to 2.9, is so close to that of quartz that no mechanical concentration can be expected in sandy sedi- ments. Instead, the beryllium minerals that may have been localized originally, as in granitic pegmatites, tend to be dispersed. Close to a rich source of beryl, a sufficient concentration may be present to make re- covery profitable; removal of other minerals in solu- tion or suspension may improve the grade. Such placer beryl has been reported from Minas Gerais, Brazil (Moraes, 1933, p. 291) where it is associated with dia- mond and tourmaline. Beryl has poor cleavage and a hardness of 7 and therefore might be expected to persist in sediments. Freise(1931) conducted experiments to show quanti- tatively the relative resistances of various minerals to abrasion. Part of his results, showing the resistance of beryl in comparison to other silicates, are tabulated below : Abrasion resistance Mineral (Hematite=100) Quartz 245 Beryl 270-465 Chrysoberyl 300 Idocrase 330 Grossularite-andradite 320-420 The many treatises on the mineralogy of sediments do not mention beryl, but this may be due to several fac- tors: (1) beryl is in the light fraction, whereas the heavy fraction is usually of greater interest to the petrographer, (2) because of dispersion the number of beryl grains will be very small except near a very rich source, and (3) grains of beryl may be mistaken for 26 apatite and possibly for quartz. Some rarer but more easily distinguished beryllium minerals such as euclase (Spencer, 1924) and gadolinite (Hutton, 1950, p. 662) have been found in clastic sediments. In finer sediments, small amounts of beryllium may occur in micas and clays. Together with some material absorbed from solution, these probably account for the small amount of beryllium found in shales. Gold- schmidt and Peters (1982, p. 367) found 0.001 percent BeQ in a composite sample of 36 shales. A detailed study of beryllium in some Italian sedi- ments was made by Pieruccini (1943; see also Carobbi and Pieruccini, 1941), the results of which are sum- marized below : Num- BeO ber of Percent sam- Rock ples High Low Average Sandstone............ 8 0.00070 0.00030 0. 00045 4 . 00056 . 000830 . 00050 Limestone._..._____... 4 . 00056 . 000836 . 00039 Pieruccini found that in coarser sediments most of the beryllium is in the cement and that the amount is larger where the cement is argillaceous. Some of the marls he tested have comparatively high beryllium con- tent ; in others the cementing calcite is low in beryllium, thus reducing the BeO content of the rock. He em- phasizes the role of source rocks in the beryllium con- tent of sediments. Although no minerals of mafic ig- neous rocks were found in the sediments that were low in beryllium, the presence of elements such as copper, cobalt, nickel, and platinum in the samples suggests these rocks as a probable source of the sediments. Few clastic sediments were sampled in the present in- vestigation, but many sedimentary rocks have been analyzed in connection with other investigations of the Geological Survey. Unfortunately, the lower limit of beryllium determination in this work was 0.001 percent BeQ, and as the analyses did not detect beryllium in the majority of samples (see table 10), they give only a rough indication of beryllium content. A large propor- tion of the samples are from phosphatic formations and associated oil shales. The oil shales contain a little more beryllium than the phosphate rock, indicating that beryllium does not tend to substitute for phosphorous in these sediments. A maximum of 0.004 percent BeO was found in each of two shale specimens of Devonian age sampled : the Helms formation north of Van Horn, Tex., and the Chattanooga shale from Tennessee. The former con- tains veinlets of gypsum, limonite, and several fine- OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES grained unidentified minerals; the mode of occurrence of the beryllium is unknown. CHEMICAL AND RESIDUAL DEPOSITS The chemistry of solution, transportation, and dep- osition of beryllium in connection with processes of weathering and sedimentation has been only partly worked out. The tendency for beryllium to follow aluminum in these processes applies only where the two metals are in solution in surface waters, and it is due to their precipitation as hydroxides under alkaline condi- tions. A similar tendency in relation to iron and man- ganese might be expected. Apparently, little beryllium is transported in surface waters under prevailing con- ditions of temperature and pH. Its concentration in sediments of chemical origin is, therefore, unlikely and is more to be expected in residual deposits, such as laterites, in which aluminum, iron, and manganese are concentrated. Strock (1941b, p. 860) found 0.001 ppm of beryl- lium in the waters of Saratoga Springs, N. Y.; the beryllium probably is nonmagmatic in origin. In dis- cussing the presence of zirconium in the same water, he postulated that it was in solution as the complex zirco- nocarbonate ion (ZrO(CO;);)~, and says (p. 868), "Beryllium should form an even more stable complex anion than ZrO, and the fact that BeCO; is formed only in presence of excess CO; and its known tendency to form soluble double salts are undoubtedly manifesta- tions of its tendency to form such stable complex anions." Although this might be admitted as a possible mode of transport of beryllium in natural waters, it is difficult to share Strock's conviction without experi- mental evidence for even the zirconium analogy. Apparently, beryllium has not been detected in sea water, but by analogy with aluminum, the expected amount would be only 10~° percent BeQ, which is well below the limit of detection. Beryllium was not de- tected in limestones analyzed in the present investiga- tion (see table 10) nor in a series of flints and other sili- ceous precipitates studied by Miropolsky and Borovick (1944). Marine sediments which may be partly clastic and partly chemical were found to contain <0.001 per- cent in some deep sea cores from the Challenger expedition (Goldschmidt and Peters, 1932, p. 367), and an average of 0.0037 percent BeO was found in three cores from the Mediterranean (Landergren, 19482). Beryllium might be expected in bauxite and clay de- posits because of its association with aluminum and with alkalic igneous rocks from which such deposits BERYLLIUM IN SEDIMENTARY ROCKS TaBug 10.-Beryllia content of sedimentary rocks, other than coal, in the United States 27 Number BeO content * Sediment Age Formation Locality of samples! High Low Average Sandstones Sandstone........_......... Devonian-Mississippian...\ Chattanooga, Hardin, Hickman and DeKalb Counties, Tenn.... $4 Ice AiG 0. 007 Maury, Meridan. Chattanooga(?).. -.--- Jackson County, Tenn....._.............- § 1 |- nou, ad cible . 004 DG. Phosphoria. . . Sweetwater County, Wyo...._.____....... 319 | <0.001 <0. 001 <. 001 Glauconitic sandstone.... .. Manasquan(?).....--- Medford, Burlington County, N. J. 47 | <.00L <. 001 <. 001 DO: vec s Harnerstone(?).......- Sewell, Gloucester County, N. J...... $4 | <.001 <. 001 <. 001 Band (titanium placers).. . . Jacksonville Beach, Fla._.._._........---- 33 | <.001 <. 001 <.001 Sand (chromite placer) ...... Cle Elum, Kittitas County, Wash.. BA <. 001 Sand (gold placer)........- Idaho County placers, Idaho...........-~- s19 | <.001 <. 001 <. 001 Sand (titanium placers).. .. Brevard County, Fla._...__.._____._....... 32 | <.001 <. 001 <. 001 Sand (tin placer).........-- Gibbonsville, Lemhi County, Idaho.. 3 | <.001 <. 001 <. 001 Sand (gold-chromite placer) . Cobs COURtY,; OTE... 43 | <.00L <. 001 <. 001 Garnetiferous sand.. ....... Fernwood, Benewah County, Idaho.... SI (enn epe cer auks . 0004 Shales Carbonaceous shale......... Pennsylvanian...........~ SVIGIOF . Haskell County, Okla......_............-- 33 0. 001 <0. 001 <0. 001 Triassic... Newark Cumnock, Lee County, N. C......_...... cue <. 001 Lignitic oil shale. .........- Elsinore, Riverside County, Calif...... a+ 31 . 004 Phosphatic shale.. ......~.- Devonian-Mississippian...! Chattanooga, Hardin, | Hickman and DeKalb Counties, Tenn.... 15 . 002 § <.001 (2) . 001 Maury, Meridan. Perinat: Phosphoria. . _.......~ Conda, Caribou County, Idaho..........- 34 | <.001 <.001 <. 001 DO-IT. seen cl caree 10; -. do-: :-40.. Lincoln County, Wyo.._....._.._........ 32 | <.001 <.001 <. 001 Do.. Upper Ordovician......... Marquoketa .... Dubuque County, Iowa................-- 3 4 . 0001 <. 0001 . 0001 Oil Chattanooga(?)- White and Jackson Counties, Tenn.... 89 .003 | 5 <.001 (8) <. 001 nes Phosphoria. . . -| Beaverhead and Powell Counties, Mont.. 3 25 .oo | $<.oo1 (19)] <.001 Siltstone ARA Shale. - .. . 1... |_ 52. Ltd aan eee nowe Canutillo. Franklin Mountains, El Paso County, 83 | <.001 <. 001 <. 001 Tex. Shale, black and oolitic. Devonian Helms.. ___| Sierra Diablo, Culberson County, Tex.... 7 .004 <. 001 .002 SHALL Cold. Lecco cecil eds. Devonian-Mississippian...| Chattanooga, Hardin, | Hickman and DeKalb Counties, Tenn.... 315 .004 8 <. 001 (12) 001 Maury, Meridan. Upper Ordovician......... CHMOR-.. 2... coun. acl B&ERYIHIG, ATI.: ... lect 111 | <.001 <. 001 <. 001 Permian..:......__...ll.. Phosphoria. _| Beaverhead and Powell Counties, Mont.. 3 52 . 001 5 <. 001 (49) <.001 Devonian | Helms.... Hueco Mts., El Paso County, Tex. AL leo ots neawnanes <. 001 Phosphoria. Sweetwater County, Wyo........ 38 | <.001 <. 001 <. 001 _____ (p. [ JL. 1 :... Li] LLLLXOGLL L Tue nei- ashnenet bee 825 | <.001 <.001 <. 001 Clay with barite. . .. Recent Sweetwater, McMinn County, Tenn.. 84 | <.001 <. 001 1 <. 001 Lignitic clay. neverse Nanfalia..-........«-« Bakerhill, Barbour County, Ala....-.-.-- 31 SA uve .002 Limestones Mississippian............~ Upper Lake Valley....| Santa Rita, Grant County, N.. Mex.:.... In ee All| aiken cus <0. 0004 D0... Ai: Pennsylvanian-Permian ..! Hueco..----.-..----- Wind Mtn., Otero County, N. Mex. I (.on nn <. 0004 Miscellaneous Residual manganese.... Shannon County, Mo...................-- SA (ei douns 0. 05 Rock Run district, Cherokee County, Als. 31 .03 Cave Springs district, Polk County, Gs.. BH (sn wie ris .02 Batesville district, Pike County, Ark.... 16 0. 01 0.008 . O1 ll. iness Early Tertiary............ Southwest Virginia district, Smythe 32 .02 .01 . O1 County, Va. DOL... enone ce | I0. I0. L. ILL Pecos cob ns nee Appalachian district, Bland County, Va.. 33 . 01 . 005 .007 Residual manganese (tail-| Cartersville district, Bartow County, Ga.. 313 . 01 . 006 009 ings). Phosphate Permian.. Phosphoria........... Beaverhead and Powell Counties, Mont.. 3 22 . 001 5 <. 001 (17) <. 001 Phosphate gravel........... PHocene:...............ss Bone Valley. Polk and Hillsborough Counties, Fla...... 37 | <.001 <.001 <. 001 Sulfur, gypsum, and salt...| ?. f pure New Gulf, Wharton County, Tex........~ 37 . 001 5 <. 001 (6) <. 001 Do. ? Reuel Plaquemines Parish, L&...._._..__......~- 11 | <.001 <. 001 <.001 1 Samples collected in the present investigation, unless otherwise noted. # BeO determined on plates exposed for general scanning, not for determination of BeO alone. 4 Concentrate or tailings sample only. was not detected. % Samples collected by the Mine, Mill, and Smelter Survey, U. S. Geological Survey. $ Number in parentheses indicates the number of analyses in which beryllium 28 commonly are derived. Samples of bauxite from vari- ous localities have been analyzed for beryllium with disappointing results, as indicated below : Locality Percent BeO Reference Jamaica......._.... 0. 05 1 Arkansas........... . 000X to 0. 0006 (!) and Goldschmidt and Peters (1982, p. 367). Hungary.........__. . 005 to 0. O1 Szelenyi (19837). Yugoslavia_________. . 0038 Minguszi (1943). France............. . OO X Goldschmidt and Peters (1932, p. 367). Halti...c........... . 0008 Goldich and Bergquist (1947, p. 76). Dominican Republic. _ . 0006 Do. Dutch Guiana____... . O01 (1) * Unpublished analyses from the files of the U. S. Geological Survey. Many of the kaolinites analyzed by Wheeler and Burkhardt (1950) are also of low beryllium content. Comparison of beryllium content of the Arkansas baux- ites and kaolinites with that of the nepheline syenites and pulaskites similar to those from which they were derived (see table 8), indicates that the beryllium was concentrated much less than aluminum, contrary to theoretical expectation. Data are as yet too few, how- ever, to support any conclusion regarding beryllium concentration in bauxites and residual clays. Landergren (1943, 1948b) determined the beryllium contents of several hundred iron ores of all types, most- ly from Sweden, but including samples from elsewhere in Europe and the United States. The lateritic iron ores of Northern Ireland were all below the limit of sensitivity-0.001 percent BeOQ. Finnish bog iron ores, which are more strictly precipitates, were also mostly below the limit. Oolitic and other marine types aver- aged 0.001 percent BeQOQ. Goldschmidt and Peters (1932, p. 368) did not detect beryllium in the few sam- ples of iron ore they analyzed, including the Clinton, N. Y., material. A sample of limonite from New Zea- land was reported to contain 0.01 percent BeO ; in an- other, beryllium was not detected (Becker and Gad- dum, 1937). Although Goldschmidt and Peters (1932, p. 368) did not detect beryllium in several samples of residual man- ganese ore, the manganese deposits sampled by the U. S. Geological Survey during World War II showed an average of about 0.01 percent BeO (see table 10). In most of these deposits the manganese came from quartz- ites and dolomites of early Paleozoic age, but they may have undergone more than one cycle of concentration (Stose and Miser, 1922, p. 52-55). Available analyses indicate no separation of beryllium between concen- trates and tailings during milling of the manganese ore. The beryllium mineral is not known. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES In the Embreeville district, Tennessee, rapid weather- ing of the Shady dolomite of Cambrian age has pro- duced minable concentrations of iron, manganese, zinc, and lead (Secrist, 1924, p. 141-145). Samples taken at the Embree mill by the U. S. Geological Survey in 1943 showed as much as 0.08 percent BeQ in the tailings and an average of 0.03 percent. Although analyses of the unweathered Shady dolomite are not available, the high beryllium content of the ore suggests that beryllium has been concentrated with the other elements during weathering. COAL DEPOSITS That beryllium tends to be concentrated in certain plants was discovered by Sestini (1888), who believed that beryllium replaced magnesium in the plant tissue. Apparently, there has been no further investigation of beryllium enrichment in plants during growth. Numer- ous analyses of coal ash indicate that beryllium tends to be concentrated during plant decomposition and coal formation. Goldschmidt (1937, p. 669) estimated beryllium to be enriched by a factor of about 50 in the average coal. The details of the enrichment process are discussed by Haberlandt (1944) who, by analogy with germanium, concludes that beryllium and other trace elements were concentrated in coal as stable organic complexes similar to porphyrin (pyrrolidine). The first comprehensive study of trace elements in coal was by Goldschmidt and Peters (1933), who found a maximum of 0.1 percent BeQO (average 0.0X percent) in ashes of coal from England and Germany. Zilber- mintz and Rusanov (1936) studied ashes of more than 600 coal samples from Russia and found 38 with more than 0.001 percent BeO; 3 contained more than 0.01 percent, and 1 contained 0.04 percent BeOQ. Similar investigations conducted by Nazarenko (1937) in Rus- sia, Lopez de Azcona and Puig (1947) in Spain, Reyn- olds (1948) in the United Kingdom, and Uzamasa (1949) in Japan and Manchuria revealed small amounts of beryllium in the ashes of coals from these countries. A summary of the literature on trace con- stituents in coal was compiled by Gibson and Selvig (1944). The beryllium content of 21 samples from a number of Colorado, Wyoming, Virginia, and West Virginia coal fields are given in table 11. i TaBu® 11.-Beryllia in ash of coals of the United States Number BeO content (percent) Age Formation Location _ samples High Low - Afsay: Late Cretaceous. Mesaverde. Colorado...___. 9 0.0025 <0.0006 0.0013 Janes do...... Wyoming...... 2 . 001 0008 . 0009 DO...«.--<-- Vermejo.... Colorado....... 3 . 0017 0006 . 0011 Do......-..c. Laramie... ._.. 2 0008 <0.0006 _ .0004 Carboniferous... _.__.__._... West Virginia.. 1 ...... . 014 coo (eeu Virginia._....... 3 01 0014 _ .004 veeciccsdcee West Virginia.. 1 -_ __.... _._...__ . 006 BERYLLIUM IN METAMORPHIC ROCKS ‘ 29 Ashes of eastern coals of Carboniferous age average 0.008 percent BeQ. Ashes of western coals of Cretace- ous age, however, average about 0.001 percent BeQO, which corresponds to the average content of shales or of igneous rocks. The reason for the different BeO contents in coals of Carboniferous and Cretaceous age and the manner of occurrence of the beryllium in the coal is not known. Beryllium has been looked for but not found in a number of marine plants (Cornu, 1919), but traces have been found in algae (Lagrane and Tchakirian, 1989). There seems to be little concentration of beryllium dur- ing the formation of petroleum, as only traces have been found in petroleum ashes (Katchenkov, 1948). BERYLLIUM IN METAMORPHIC ROCKS Only isochemical metamorphic rocks (those which have not received metasomatic additions of material while being changed by heat and pressure) are included under this heading. Some cale-silicate rocks which may belong in this category are discussed with the pyrometa- somatic deposits, with which they are associated. Meta- morphic rocks as thus defined would be expected to show little difference in composition from the sedimentary or igneous rocks from which they were derived. Local concentrations of beryllium by the processes of meta- morphic differentiation are conceivable but probably rare. Analyses for beryllium have been made of a large number of schists and gneisses from a wide range of metamorphic facies, principally in Finland (Sahama, 19452, p. 38-39), Sweden (Landergren, 1948b, p. 77-78), and Greenland (Wager and Mitchell, 1943, p. 286-287). In more than 80 percent of these rocks the content was below the limits of detection; which ranged from 0.003 to 0.0003 percent BeQ. Of those in which beryllium was detected, quartz-biotite schist from the Striberg iron district in Sweden contained 0.011 percent BeQ, but the rest were below 0.005 percent. No rocks of this type were sampled during the present investigation; a few recent analyses of metamorphic rocks by the Geo- logical Survey show little or no BeQ. BERYLLIUM IN PYROMETASOMATIC AND RELATED DEPOSITS PREVIOUS AND PRESENT INVESTIGATIONS Pyrometasomatic deposits containing beryllium were first described by Goldschmidt (1911) in his monu- mental work on the metamorphic rocks of the region around Oslo, Norway. Helvite is associated with gar- net, idocrase, diopside, magnetite, fluorite, and other minerals in these deposits, which were regarded as hav- ing little commercial value. Helvite was also reported in pyrometasomatic deposits at Lupikko, Finland (Trustedt, 1907), Schwarzenburg, Germany (Beck, 1904), Bartlett, N. H. (Huntington, 1880), and Casa La Plata, Argentina (Fischer, 1925; 1926). Gold- schmidt and Peters (1932) devoted a great deal of their study of the geochemistry of beryllium to this type of rock. Landergren (1948b) determined beryllium in several pyrometasomatic deposits in Sweden. The ana- lytical results for European localities are given in table 12. The discovery of idocrase of high beryllian content Tasos 12.-Beryllia in pyrometasomatic rocks from Germany, Norway, and Sweden [All analyses of rocks from Sweden from Landergren (1948b),! others from Gold- schmidt and Peters (1932)] Number BeO (percent) Description Locality smgples High Average Skarn*-magnetite . Nordmark region, 6 0.03 0. O1 Sweden. Banded quartz- Skinnskatteberg 12 . 03 . O1 hematite, skarn- region, Sweden. magnetite, sul- fides. Quartz-magnetite, - Silvberg-Sater 6 . 03 . 01 skarn-hematite. region, Sweden. Grossularite *- Thale-Friedrichs- 1: . O1 diopside-wollas- - brunn, Germany. tonite hornfels. Grossularite 3- Braulage, Ger- I ---> . OL diopside-an- many. orthite hornfels. Skarn-magnetite, _ Persberg region, 6 . 02 . 007 cummingtonite. Sweden. Calcite-magnetite, - Norberg region, 17 . 03 . 007 quartz-hematite, Sweden. actinolite-skarn- magnetite, others. Skarn-magnetite. . Upspland region, 12 . 02 . 006 weden. Calcite-magnetite. - Stallberg, Sweden. 2 . 008 . 006 Diopside-skarn- Garpenberg region, 7. . 02 . 004 magnetite. Sweden. Skarn-magnetite, _ Sodermanland re- 4 . 008 . 004 quartz-magne- gion, Sweden. tite. Amphibole skarn, _ Nora-Viker re- 4 . 03 . 004 cummingtonite gion, Sweden. skarn, quartz- amphibole skarn. Anorthite-cordi- Thale-Friedrichs- 1 .-- . O01 erite hornfels. brunn, Ger- many. Anorthite-diopside - Aarvold-Grorud, $ i.... . 001 hornfels. Norway. Grossularite-diop- - Aro, Norway___-- 1 ...--...- . OO1 side hornfels. Skarn-magnetite.. Grythyttan re- 4 <.003 <. 003 gion, Sweden. Manganoan oli- Ljusnarsberg re- 9 <.003 <.003 vine, magnetite, gion, Sweden. mica, others. Skarn-magnetite, Norrbarke region, 3 <.003 <.003 quartz-skarn- Sweden. magnetite. Anorthite-hyper- _ Aarvold, Norway. ¥. ...... <. 001 sthene hornfels. Andradite skarn .. Grua, Norway... 2 . <. 001 _ «<. 001 1 A total of 150 analyses, mostly of gangue from pyrometasomatic iron deposits. Some metamorphosed quartz-iron sediments included where associated with silicates. Minimum content 0.003 percent BeQ at all localities, |. 2 Skarn is a type of tactite, generally rich in andradite and hedenbergite. 3 Grossularite or idocrase or both. 30 at Franklin, N. J. (Palache and Bauer, 1930, p. 31) raised hopes that idocrase in other deposits might be similarly rich in beryllium; however, Zilbermintz and Roschkova (1933) showed that beryllian idocrase occurs only rarely. Interest in pyrometasomatic beryllium was revived by the discovery of helvite at Iron Mountain, N. Mex. (Strock, 1941a). In a detailed survey of this deposit, Jahns (1944a; 1944b) found that beryllium occurred in greatest amount as helvite associated with magnetite OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES and fluorite, in a tactite having a finely banded struc- ture of diffusion-replacement origin ("ribbon rock"). Other tactites rich in magnetite, fluorite, grossularite, idocrase, and other silicates contain less beryllium. Although the deposit at Iron Mountain is not ore at present, it has focused attention on tactite deposits as potential sources of beryllium. The present investiga- tion included sampling of a large number of pyrometa- somatic deposits in the western United States. The results are summarized in table 13, along with some TaBu® 13.-Beryllia content of some pyrometasomatic and related deposits of the United States Number BeO content Locality of Mineralogy ? Associated metals ®| Associated intrusive samples ! rocks 2 High Low Average Bartlett, Carroll County, N. H...... 32 1.6 1.0 1.5 Magnetite, hematite, danalite, galena | Fe, Granite. chalcopyrite, fluorite, quartz. Iron Mtn., Sierra County, N. Mex.... (8) 3.5 .4 -T Magnetite, fluorite, helvite._......_____ Be, Fe,. W...... Granite. Do. . i.. led en ee anes ln nud seee (4) . 85 1 h Grossularite (0.19), idocrase (1.09), |.______._____________ helvite, fluorite, chlorite. Magnet Cove, Hot Springs County, T| irene ten Pesi .028 | Idocrase (0.04), phlogopite......__..... Nepheline syenite. Ark. Star mine, Elko County, Nev.......... 3 . 056 . 0044 .027 | Garnet, diopside, epidote, quartz, | W._.._____________. Biotite granite, quartz calcite, scheelite. monzonite. Mill Creek, Anaconda, Mont......_._.. Een eis. ine. .022 | Idocrase, fluorite, calcite, hedenbergite, Diorite. biotite. Dragoon Mts., Cochise County, Ariz.... 4 . 04 . 004 5,02 Garnet, epidote, hematite, galena, Granite. sphalerite. - Victorio Mts. district, Luna County, 10 VA . 003 .02 Garnet, calcite, helvite, serpentine, Rhyolite porphyry. N. Mex, idocrase (0.2), fluorite. Victory tungsten deposits, Mammoth I Lele ere EAL aks .014 | Biotite, chlorite, amphibole(?), pyrox- Granodiorite. Range, Nye County, Nev. ene(?). Drumlummon mine, Marysville, Mont. I .O11 | Quartz, garnet, mica, feldspar...._____ Quartz monzonite. Carpenter district, Grant County, N. 9 . 02 <. 001 . 01 Quartz, fluorite, galena, sphalerite, Do. Mex. garnet, chlorite, helvite. Gallinas district, Lincoln County, N. $A {cus geese §.008 | Magnetite, actinolite._....._._____.___ Fo...... Arc Syenite porphyry. Mex. Rose Creek, Pershing County, Nev.... 6 . 024 . 0032 .0078 | Diopside, actinolite, feldspar, quartz, | W....____.______.. Granite to diorite. * scheelite, pyrite. Capitan district, Lincoln County, N. A eel» 5.005 | Muscovite, tremolite..._.......___.___ ''Aplite." Mex. Wind Mtn., Otero County, N. Mex.... 10 . 026 <. 001 .005 | Aegerite, riebeckite, feldspar, eudialite, | Be______._________ Nepheline syenite peg- wollastonite, garnet. matites. Cave Peak, Culberson County, Tex.... 3 . 0005 <. 004 <.004 | Spurrite, merwinite; epidote, calcite, | W, Be._____.____.. Granite and rhyolite. ; garnet, idocrase. Marble Canyon, Culberson County, 7T | <.004 <. 004 <.004 | Brucite, calcite, quartz, diopside, | Nome..___________. Syenite. Tex. akermanite, wollastonite. Quitman Mts., Hudspeth County, 9 | <.004 <. 004 <.004 | Garnet, actinolite, epidote, hematite, | Cu, W, Pb...__... Quartz monzonite. Tex. quartz, idocrase. Sierra Prieta, Hudspeth County, Tex... 2] <.004 <. 004 <.004 | Calcite, unidentified silicates.._______. Phonolite. Panther Canyon area, Humboldt 12 . 0078 <. 0001 0023 | Diopside, idocrase, feldspar, epidote, | None.....__.______ Aplite, granite por- Range, Pershing County, Nev. tremolite, others. phyry. Nevada-Massachusetts Co. mines, 30 . 004 <. 0001 .002 | Garnet, epidote, quartz, calcite, schee- | W....__________.__ Granodiorite. Mill City district, Pershing County, lite. Nev. Franklin district, Sussex County, N. J. 7110 . 003 <. 0004 , 002 Willemite (0.005), franklinite, calcite, | Zm_.______________ Granite pegmatite. garnet, diopside (0.01), zincite, rare idocrase (3.95), and barylite. Oreana mine, Humboldt Range, Per- 3 . 0031 . 0008 .0018 | 'Tactite and silicated marble"....__.. Aplite, pegmatite. shing County, Nev. Pine Creek mine, Inyo County, Calif... 5 , 0087 <. 0001 .0017 | Garnet, diopside, epidote, quartz, | W, Mo...________. Quartz diorite. feldspar, scheelite, molybdenite. Ragged Top mine, Trinity Range, 5 . 0019 <. 0001 .0013 | Garnet, diopside, scheelite....._._.... W Leen lh 22s Granodiorite. Pershing County, Nev. Johnson district, Cochise County, Ariz. 112 . 005 <. 0004 .001 | Garnet, diopside, epidote, chalcopy- | Cu_._____________. Quartz monzonite. rite, sphalerite, idocrase (0.005). Burro Mts., Grant County, N. Mex.... 11 5.001 | Silicates, scheelite_._._______.______... W- cade is caren Quartz monzonite(?). Bisbee, Cochise County, Ariz...._..... 891 5<.001 | Calcite, pyrite, tremolite, diopside, | Cu_____________.. Granite porphyry. chalcopyrite. Christmas mine, Gila County, Ariz.... $301 .s avea ireul. lou §<.001 | Garnet, idocrase, epidote, quartz, | Cu_..._________.. Quartz diorite. See footnotes at end of table. magnetite, pyrite, chalcopyrite. BERYLLIUM IN PYROMETASOMATIC AND RELATED DEPOSITS 31 TaBu® 13.-Beryllia content of some pyrometasomatic and related deposits of the United States-Continued Number BeO content Locality 0 Mineralogy ? Associated metals *| Associated intrusive samples ! rocks 2 High Low Average Ajo, Pima County, Ariz......~. au $4 [oo. ei 5<0.001 | Chlorite, epidote, sericite, orthoclase, | Cu._._.___...--.---- Quartz monzonite. chalcopyrite, pyrite. Control mines, Oracle, Pima County, Milo.; 5<.001 | Calcite, garnet, epidote, quartz, chal- | Cu, Pb, Zn.....-- Hornblende diorite. Ariz. copyrite, galena, sphalerite. Greenhorn Mts., Kern County, Calif... #3 | <0. 001 <0. 001 s<.001 | Quartz, biotite, garnet, epidote; wol- | W, Mo....._.....~ Granodiorite. lastonite, scheelite, pyrrhotite. Darwin, Inyo County, Calif............ a3 | <.001 <. 001 5<.001 | Wollastonite, idocrase, grossularite, | W, Pb, Ag...----- Quartz diorite. epidote, scheelite, pyrite, fluorite. Tungsten Hills, Inyo County, Calif.... 27 . 0045 <. 0001 <.001 | Quartz, calcite, garnet, epidote, schee- | W...........------ Granite, quartz mon- lite. zonite. Calumet mine, Chaffee County, Colo... 7 | <.001 <. 001 <.001 | Garnet, magnetite, actinolite, epidote, | Granodiorite. kaolinite, calcite, quartz, pyrite. Monarch mining district, Chaffee 6 | <.o01 <. 001 <.001 | Garnet, epidote, quartz, calcite, | Au-_______.___-.-- Quartz monzonite. County, Colo. pyrite, limonite. Grayback mining district, Costilla 3 | <.o01 <. 001 <.001 | Garnet, epidote, actinolite, diopside, | Au..._.....-.------ Monzonite porphyry. County, Colo. magnetite. ; Italian Mtn., Gunnison County, Colo.. 11 . 0013 <. 0001 <.001 | Garnet, actinolite, graphite, quartz, | Au-._____-..-.---.-- Quartz monzonite. idocrase. Snowmass Mtn. area, - Gunnison 8 | <.o01 <. 001 <.001 | Garnet, epidote, hematite, pyrite, | Nome.....____...-- Granite County, Colo. quartz, calcite, diopside. Tomichi Mining district, Gunnison 19 | <.001 <. 001 <.001 | Garnet, epidote, magnetite, pyrite, | Pb, Zn, Ag......-- Quartz monzonite. County, Colo. chalcopyrite, galena, sphalerite. Rico mining district, Montezuma P epl <.001 | Garnet, epidote, galena, sphalerite, | Pb, Zn...........- Do. County, Colo. chlorite. Breckenridge mining district, Summit 3 | <.001 <. 001 <.001 | Garnet, epidote, magnetite, pyrite_...! Au-..___.._.....-- Quartz monzonite por» County, Colo. phyry. Mackay district, Custer County, Idaho. $4 | <.001 <. 001 5 <.001 | Andradite, chalcopyrite, pyroxene, py-| Cu-____...._._...-- Granite porphyry. rite, pyrrhotite, fluorite, magnetite. Georgetown district, Deer Lodge 71 <.001 <. 001 <.001 | Magnetite, olivine, dolomite, horn- | Fe, Au, Granodiorite. County, Mont. blende, epidote. Garnet district, Granite County, Mont. 2 | <.001 <. 001 <.001 | Garnet, diopside, magnetite...._...... Au, Cu- Do. Philipsburg district, Granite County, 3 | <.001 <. 001 <.001 | Calcite, quartz, pyrolusite, magnetite, | Mn, Ag_....------ Do. Mont. * serpentine. Red Lion district, Granite County, % | <.00 <. 001 <.001 | Quartz, limonite, sericite, dolomite....] Au...._.......---- Do. Mont. Edwards, St. Lawrence County, N. Y. SAL {.! ber ead 5 <.001 | Calcite, diopside, tremolite, pyrite, | Zn...__.....------ Granitic pegmatite. sphalerite, willemite. Cornwall, Lebanon County, Pa......-- #3 | <.001 <. 001 § <.001 | Magnetite, diopside, actinolite, phlo- | Fe, Cu, Co......-- Quartz diabase. gopite, calcite. West Tintic mining district, Juab and #3 | <.001 <. 001 5 <.001 | Magnetite, specularite, garnet, epidote,| Au, Ag, W..---..- Quartz monzonite and Utah Counties, Utah. diopside, tremolite, quartz, scheelite. granodiorite. Tintic mining district, Juab County, 85 | <.001 <. 001 5 <.001 | Magnetite, specularite, quartz, epi- | Au, Ag, To...... Quartz monzonite. Utah. dote, garnet, diopside. Little Cottonwood mining district, #2 | <.001 <. 001 5 <.001 | Idocrase, quartz, garnet..____._______-- Ag, Ou, Pb.:..... Do. Salt Lake County, Utah. Ophir mining district, Tooele County, $A | reine cre eeu ne anne $.001 | Marbic.epidofe...l.....-.......-...«« PD, Monzonite and lam- Utah. porphyre dikes. Garfield Peak, Natrona County, Wyo.. I |All <, -| Quartz, Latite. Bayard, Grant County, N. Mex.......~ 5 .002 | # <.0004 (1)| 5.0009 | Hedenbergite, sphalerite, pyrite, tho- Quartz monzonite. donite, garnet. Mt. Silver Heels, Como, Colo.........- 3 . 0010 . 0004 .0008 | Magnetite, garnet, epidote............ Do. Cuchillo Negro district, Sierra County, 3 . O01 . 0005 5.0007 | Calcite, garnet, epidote, quartz, galena, Granite (?). N. Mex. sphalerite. Morenci, Greenlee County, Ariz........ 8 2 . 0005 <. 0001 5 <.0005 | Andradite, diopside, tremolite, pyrite, Diorite to granite por- magnetite, chalcopyrite. phyries. Sybille Creek, Wheatland, Wyo.......- 6 . 0013 <. 0001 .0005 | Sericite, actinolite, idocrase, calcite, Granite. biotite, garnet. Hornet mine, Rio Arribs County, 2 . 0008 <. 0003 5.0004 | Quartz, calcite, garnet, pyrite, galena, Granodiorite. N. Mex. sphalerite. Sedalia mine, Chaffee County, Colo.... I .0004 | Actinolite, idocrase, garnet, sphene, None. pyrite. Courtland, Cochise County, Ariz...._.. 2 | <.0004 <. 0004 5 <.0004 | Garnet, epidote, pyrite, chalcopyrite! Cu.__.____._...-..-- Quartz monzonite. Tombstone, Cochise County, Ariz...... 4 . 0007 <. 0004 5 <.0004 | Garnet, calcite, tremolite, idocrase..... Ag, Pb, Cu, Mn.! Granodiorite. Empire district, Pima County, Ariz.... 4 | <.0004 <. 0004 s <.0004 | Garnet, diopside, quartz, calcite; | W._...___.__._._------ Quartz monzonite. wollastonite. Helvetia, Pima County, Ariz.._.__....- 9 . 002 <. 0004 5 <.0004 | Garnet, diopside, chalcopyrite........- oce Granite and alaskite porphyries and aplites. Mineral Hill and Twin Buttes districts, 14 . OOL <. 0004 5 <.0004 | Garnet, quartz, epidote, pyrite........ Zn, Pb, Cu, W....| Granodiorite, granite. Pima County, Ariz. Patagonia district, Santa Cruz County, 9 | <.0004 <. 0004 § <.0004 | Garnet, quartz, chalcopyrite, galena, | Cu, Pb, Zn-_.---- Quartz monzonite and Ariz. sphalerite. granite porphyry. See footnotes at end of table. 32 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Tapur 18.-Beryllia content of some pyrometasomatic and related deposits of the United States-Continued Number BeO content Locality of Mineralogy Associated metals ?} Associated intrusive samples ! rocks 2 High Low Average Cimarroncito district, Colfax County, 4 | <0.0004 |<0.0004 |5<0.0004 | Garnet, diopside, hematite, horn- | CU_______________ Quartz monzonite. N. Mex. blende, pyrite, chalcopyrite. Elizabethtown, Colfax County, N. Mex. 3 | <.0004 | <.0004 5 <.0004 | Diopside, hornblende, seapolite(?)..... ces Monzonite porphyry. DO AA CeCe veneer 3 . 0004 19} <.0004 (2)] 5 <. 0004 Epidote, hematite Do. Organ Mts., Dona Ana County, 9 0004 *! <.0004 (8)] 5 <.0004 | Garnet, quartz, hematite, sphalerite, Monzonite to quartz N. Mex. altaite. monzonite. Eureka district, Grant County, N. Mex. 7 | <.0004 <. 0004 5 <.0004 | Garnet, pyroxene, chalcopyrite.._.____ Monzonite. Fierro, Grant County, N. Mex......... 1 (freer | dees 5 <. 0004 Magnetite, serpentine...._.___________ Quartz monzonite. Hanover, Grant County, N. Mex._..... 10 0008 19} <.0004 (8)| 5 <.0004 | Garnet, hedenbergite, epidote, mag- Do. \ netite, ilvaite, pyrite, sphalerite. Pinos Altos, Grant County, N. Mex... 2 | <.0004 <. 0004 5 <.0004 | Calcite, sphalerite, pyrite, chalco- Granodiorite. pyrite. Santa Rita, Grant County, N. Mex.... 10 . 001 <. 0004 5 <.0004 | Epidote, garnet, pyrite, chalcopyrite, | Cu, Zn-.__________ Quartz monzonite. magnetite. Apache Hills, Hidalgo County, 4 | <.0004 <. 0004 5 <.0004 | Garnet, epidote, pyrite. Cg, Quartz monzonite por- N. Mex. a phyry. Peloncillo Mts., Hidalgo County, 3 | <.0004 <. 0004 5 <.0004 | Garnet, galena, Ph, Za...... Monzonite porphyry. N. Mex. Jones Camp district, N. Mex.._________ $4 |.. nese $0004 | 002.2 in Diabase. Tres Hermanas Mts., Luna County, 2 | <.0004 <. 0004 5 <.0004 | Garnet, amphibole, calcite.. ___.... : .es s Granite porphyry. N. Mex. Ortiz district, Santa Fe County, N. Mex. 2 | <.0004 <. 0004 5 <.0004 | Garnet, hornblende...._.___.____.__.... Syenite. San Pedro district, Santa Fe County, 11 | <.0004 <. 0004 5 <.0004 | Garnet, calcite, hornblende, epidote...| CU, W...... Do. N. Mex. d Potosi district, Humboldt County, Nev. 85 . 0003 <. 0001 0003 | Epidote, quartz, garnet, scheelite._.._. Granodiorite. Rawhide district, Mineral County, Nev. 12 . 0028 <. 0001 0002 | "'Tactite and hornfels"._______________ Granite. Ouray mining district, Ouray County, 2 . 0002 . 0002 0002 | Garnet, magnetite, epidote, quartz, Quartz monzonite. Colo. limonite. Beaver-Tarryall mining district, Park 7 . 0001 . O01 0001 | Garnet, epidote, magnetite, quartz, Do. County, Colo. calcite, phlogopite. Geneva claims, Chaffee County, Colo... 3 | <.0001 <. 0001 <.0001 | Molybdenite, garnet, pyrite, galens, | Mo............... Granite. calcite. Georgetown area, Clear Creek County, A Ire saban be oar ane £.0001 | Garnet, epidote. ..c.......0..02....... Do. Colo. Gold Brick mining district, Gunnison 2 | <.0001 <. 0001 <.0001 | Garnet, magnetite, quartz, pyrite, | AU_____________.__- Diorite and granite. County, Colo. chalcopyrite. Tincup mining district, Gunnison 3 | <.0001 <. 0001 <.0001 | Magnetite, garnet, specularite, epi- | Fe---.___-_-_----- Quartz diorite. County, Colo. dote. Rush Basin area, Montezuma County, J <.0001 | Garnet, specularite, epidote, quartz.._| Nome........__.... Monzonite. Colo. Montezuma mining district, Summit 2 | <.0001 <. 0001 <.0001 | Garnet, epidote, quartz, sulfides...____ AU-+ Quartz monzonite. County, Colo. Toll Mountain area, Deer Lodge I (sere [eras cau <.0001 | Garnet, diopside, hedenbergite..._.... Granite. County, Mont. Neihart-Yogo Peak area, Cascade 3 | <.0001 <. 0001 <.0001 | Pyroxene, epidote, garnet, calcite, | Lamprophyre. County, Mont. prehnite, thomsonite, orthoclase, idocrase, magnetite, wollastonite, sphene, eudialite, merwinite. Elkhorn mining district, Jefferson 3 | <.0001 <. 0001 <.0001 | Epidote, garnet, pyrrhotite, caléite, | Pb, Zn....... -.... Granite. County, Mont. scapolite. Spring Hills mine, Lewis and Clark P <.0001 | Garnet, olivine, seapolite, titanite, | AU._______________ Diorite. Counties, Mont. epidote. Silver Star mining district, Madison 2 { <©.0001 <. 0001 <. 0001 Hedenbergite, garnet, epidote, horn- | Au..______.____... Granite. County, Mont. blende, calcite, magnetite, pyrrho- tite. Ophir mining district, Powell County, I {ee five nee e <.0001 | Garnet, epidote, calcite..........__.... veg Quartz monzonite. Mont. Priests Pass area, Powell County, Jo [ne neuer ce nases <. 000L | Garnet; MMA ACCEL O- Do. Mont. Highland mining district, Silver Bow 2 | <.0001 <. 0001 <.0001 | Garnet, epidote, magnetite, diopside, | AU.____________.__ Diorite and quartz County, Mont. actinolite, pyrite, chalcopyrite. monzonite. Haystack Stock, Sweet Grass County, L neice ne <.0001 | Garnet, epidote, quartz, actinolite...._ Quartz monzonite. Mont. ! Samples collected by the U. S. Geological Survey during the present investigation, unless otherwise noted. 2 Minerals, metals, and intrusive rocks spacially associated in the mineral deposit, not necessarily related in time or genesis. Known beryllium-bearing minerals in italics, their maximum beryllium content for that deposit in parentheses. * Samples collected by D. M. Henderson, University of Illinois. 4 Data from Jahns (19448, p. -, 76). 5 Determinations on plates for general scanning, not for precise determination o BeO alone. 6 Samples collected by V. C. Kelley, U. S. Geological Survey. " Samples furnished through courtesy of the New Jersey Zinc Co. 8 Samples collected by Mine, Mill, and Smelter Survey, U. S. Geological Survey. * Tailings or slag samples only. ¢ Numbers in parentheses indicate number of samples having a BeO content below limit of sensitivity. 11 Six of the samples collected by J. R. Cooper, U. S. Geological Survey. !? Sample collected by Elliot Gillerman, U. S. Geological Survey. BERYLLIUM IN PYROMETASOMATIC AND RELATED DEPOSITS 33 earlier determinations from the files of the U. S. Geo- logical Survey. The minerals, metals, and intrusive rocks of each deposit are also tabulated, although in most places they probably are unrelated in origin and time of deposition to the beryllium. Extensive sampling shows that only a small number of pyrometasomatic deposits contain more than 0.001 percent BeQO, the average for the earth's crust. Only 15 percent of the United States deposits sampled con- tain more than 0.005 percent BeQ. The Swedish de- posits are of somewhat better grade. In most of the pyrometasomatic deposits that have been analyzed throughout the world, beryllium was not detected. CHARACTERISTICS OF BERYLLIUM-BEARING DEPOSITS Some of the common minerals in the beryllium-bear- ing pyrometasomatic rocks are helvite, idocrase, garnet (mostly andradite), magnetite, fluorite, scheelite, and diopside-hedenbergite. Theoretically, these minerals may form in any metamorphic temperature and pres- sure facies from "pyroxene hornfels" down to "epidote amphibolite" (Turner, 1948, p. 70-90). Paragenetic data from the few deposits studied in detail indicate that deposition of helvite is possible through this en- tire range of temperature. Idocrase commonly is associated with helvite in beryllium-bearing tactites. (See table 13; also tables 12 and 13 of Glass, Jahns, and Stevens, 1944). Be- cause grossularite and idocrase are similar in structure and composition, although idocrase is slightly poorer in aluminum, one might wonder why beryllium occurs in idocrase-bearing tactites in preference to grossula- rite-bearing tactites. Idocrase in normal metamor- phosed limestones may form in equilibrium with gross- ularite and diopside, grossularite and calcite, or diop- side and calcite (wollastonite may take the place of calcite at higher temperatures), but only if the com- position of the rock is less aluminous than grossularite itself (Turner, 1948, p. 91). Holser (1953, p. 607) has noted in Victorio Mountains, N. Mex., that helvite forms in rocks having relative low alumina content. At Rose Creek, Nev., beryllium occurs without the aluminum garnet (grossularite), the principal minerals being diopside, actinolite, and feldspar. Thus, among metamorphosed limestones, beryllium is more likely to be found in those that were originally low in argilla- ceous material and to which little alumina has been added in the metamorphic process. Actually, the nature of equilibrium relations be- tween idocrase and grossularite is in some doubt. Kerr (1946a, p. 58) observes that both minerals form after 467945-59--4 marmorization of limestone but before intense replace- ment. According to Osborne (1932, p. 221-222), ido- crase may be "generated during retrogressive meta- morphism with which was associated a change pro- moted by falling temperature, and at pressures under which grossular was not stable. . . The data available concerning the various grades suggest that while this mineral may occur with grossular and wollastonite, if is also stable in a lower grade where these two minerals fail to develop." The nature of the implied pressure change is not discussed. Tilley (1927, p. 375) sug- gested that both idocrase and grossularite might form at lower temperatures than normal when subjected to the shearing stresses of regional metamorphism. A further reason for the association of beryllium and idocrase may be due to fluorine. Fluorine-rich idocrase and fluorite are common minerals in beryllium-bearing deposits and thus may be a clue to the occurrence of helvite or other beryllium minerals. Although the ido- crase-fluorite association is not found in all pyrometa- somatic deposits containing beryllium, the Darwin, Calif., deposit is the only one sampled at which these minerals were found without beryllium. Idocrase with- out fluorite or beryllium was found at several localities. In the Carlingford district, Ireland, are several varie- ties of idocrase, some associated with simple isochem- ically metamorphosed limestones, and others associated with "pneumatolytic" alteration around pegmatites. Regarding the associations, Osborne (1982, p. 222) says, "Where pneumatalytic metamporhism operates in an aureole, fluorine, if available, enters the constitution of vesuvianite, but it is suggested here that vesuvianite which is due entirely to diaphoretic changes * * * will be fluorine free." The implication that fluorine-rich idocrase and associated products are of pneumatolytic origin may be valid. In the absence of experimental data the nature of the beryllium-fluorine relations in pyrometasomatic deposits remains con] ectural. Magnetite and scheelite are commonly found in de- posits containing beryllium minerals. In most of the de- posits, however, helvite formed later than magnetite, mainly in open cavities. At Iron Mountain, N. Mex., scheelite is also earlier than helvite. The helvite in tactite in the Victorio Mountains may be exceptional (Holser, 1953, p. 606) in that it appears to be contem- poraneous with the other silicates and to have formed at relatively high temperature. Scheelite is present but magnetite is not. Most of the Nevada and California scheelite-bearing tactite deposits sampled during the present investiga- tion contain more beryllium than the average pyrometa- somatic deposit (see table 13). As yet the beryllium- bearing minerals in these deposits and their positions 34 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES in the mineral sequence are not known. The relation between beryllium and iron or tungsten, although not clearly defined, is in marked contrast to the negative correlation of beryllium with copper, zinc, or lead. Landergren (1948b) found little correlation between type of ore and beryllium content in the pyrometaso- matic iron deposits of Sweden. In the United States, however, beryllium was not found in deposits contain- ing magnetite with olivine or derived serpentine like those at Fierro, N. Mex. The lack of beryllium can hardly be due to an excess of magnesium, as magnesium- rich pyroxene or amphibole is a common associate of beryllium-bearing pyrometasomatic deposits and may occur in such a deposit to the exclusion of garnet. The fact that olivine normally forms at higher temperatures than pyroxene or amphibole may account for the ap- parent lack of correlation between olivine and beryllium in these deposits. Jahns (1944b, p. 179-189) suggests that the banded and orbicular structures observed at Iron Mountain, N. Mex., may be a clue to the presence of beryllium in tac- tite. He notes that similar tactite were previously de- scribed from Seward, Alaska, and Pitkaranta, Finland. The former was tested and found to contain beryllium. In the latter area, helvite occurs in intimate association with idocrase and fluorite (Trustedt, 1907) ; the idocrase has been found to contain 0.18 percent BeOQ (Zilber- mintz and Roschkova, 1933, p. 253). None of the beryl- lium-bearing tactite sampled in the present investiga- tion showed banding of this type, but banded and or- bicular structures are common in magnetite-serpentine rocks that lack beryllium, as at Philipsburg, Mont., and in the Quitman Mountains, Tex. . Jahns (1944b, p. 196-204) postulates that the banded beryllium-bearing tactite is of hydrothermal origin, in contrast to massive tactites of simpler mineralogy, which may be pneumatolytic. He infers that the latter are less likely to contain beryllium. The helvite deposit in the Victorio Mountains, N. Mex., is massive and of sim- ple mineralogical composition. The difficulty of dis- tinguishing the actions of liquid and gaseous solutions at high temperature does not exclude the possibility that even this deposit may be hydrothermal. Whatever the details of their origin, such massive tactite cannot be excluded as possible sources of beryllium. Results of analyses show that simple metamorphic hornfels, quartzite, and marbles that surround tactite deposits are notably lacking in beryllium. It must be presumed to have been added to the tactite, along with other constituents, by solution probably derived from an igneous source. The commonly held theories of mag- matic differentiation imply that beryllium should be concentrated with late products of differentiation, such as granite or nepheline syenite and associated pyro- metasomatic deposits Actually beryllium-bearing pyrometasomatic deposits are more commonly associ- ated with rocks of intermediate composition, such as granodiorite and monzonite. Though some beryllium is found in the contact zone of feldspathoidal intrusive rocks, the tactite zones adjacent to these rocks gener- ally are small and poorly developed. RELATED OCCURRENCES Helvite at the Grandview mine, Carpenter district, New Mexico (Weissenborn, 1948), is nearly all found as sharp, tiny tetrahedra on quartz and fluorite crystals in vugs and in veins. In some places the quartz was coated with chalcedony before deposition of the helvite. Although a small amount of garnet and other silicates are found replacing the limestone in the Grandview mine, the manner of occurrence suggests that the helvite is a low-temperature mineral, more closely related to vein filling than to pyrometasomatism. The zinc deposits at Franklin and Sterling Hill, N. J., bear little relation to any other deposits in the world, with the possible exception of those at Langban, Swe- den (Palache, 1929b). The rare mineral barylite has been found at only these two New Jersey localities. Brown idocrase, similar to that in which a large amount of beryllium has been found, is of rare occurrence in the Franklin mine, and the blue variety (cyprine), which contains a small amount of beryllium, is even rarer. Palache (19299, p. 10-11) believed that these minerals were a product of pneumatolytic action around intruded late pegmatites. No beryl has been found in the pegmatites, or elsewhere in the district. A large amount of beryllium at low concentration is contained in the great masses of willemite and associ- ated zincian-manganian diopside. The pegmatites were formed after deposition of willemite and may have reconcentrated a little beryllium in their vicinity. It is a mystery why some of the beryllium does not occur as helvite, especially because of the excess of manga- nese, zinc, and iron. Beryl is found in mica and amphibole schists at the Izumrudnie (emerald) district of the southern Urals (Fersman, 1929, p. 74-116) ; Habachtal, Salzburg, Aus- tria (Koenigsberger, 1913) ; Leydsdorp, South Africa (Le Grange, 1930) ; Keene, N. H. (Olson, 1942, p. 872) ; and the Black Hills, S. Dak. (Page and others, 1953, p. 46). At all of the localities for which detailed geo- logic description is available, the beryl is near granitic pegmatites that are beryl-bearing. At the Tungsten King mine, Arizona, beryl occurs in the chlorite schist in the hanging wall of the quartz-beryl-tungsten vein. More remarkable are two similar occurrences in which BERYLLIUM IN VEIN DEPOSITS the beryl is in marble (Just, 1926; Chhibber, 1945). Studies of these deposits indicate that the beryllium has been added to the wall rock from the pegmatite or vein (see also Stoll, 1945). Apparently, this mode of oc- currence is rare for beryl, as most beryl pegmatites do not introduce beryllium into the wall rock even in trace amounts. In most of the deposits mentioned, the beryl in the wall rock is much less abundant than in the as- sociated pegmatites. With the exception of the Urals deposits, which are quite large, they are of little eco- nomic importance unless the beryl is of gem quality. BERYLLIUM IN VEIN DEPOSITS Beryllium minerals, chiefly beryl or helvite, have been found sparsely disseminated in certain types of veins. Such veins generally contain ores of useful metals and are thus well suited to recovery of beryllium as a by- product. The published descriptions of beryl-bearing veins are tabulated and discussed by Holser (1953, p. 604-605 and Adams, 1953). More than 100 high-tem- perature veins in the western United States were sam- pled and analyzed for beryllium. Previously, a large number of vein samples collected by the U. S. Geologi- cal Survey had been analyzed qualitatively. These analytical data are summarized in table 14. Analyses for several miscellaneous deposits that are not strictly veinlike are included in the table. Those veins in which beryllium minerals have been noted, as well as those in which beryllium was found by sampling, fall largely into three groups: quartz-tung- sten veins; quartz-gold veins; and manganese-lead-zinc veins. QUARTZ-TUNGSTEN VEINS Beryllium appears to be more common in quartz- tungsten veins than in other kinds of veins, the asso- ciation having been noted at a dozen or more localities throughout the world. In some deposits, as exemplified by the Boriana mine, Mohave County, Ariz. (Hobbs, 1944, p. 254), the quartz veins contain fluorite, wol- framite, and sulfides. Generally, beryllium occurs in beryl, which is found only in small amounts. In some veins of this type the beryl may be altered to phenakite er bertrandite, but no helvite has been noted. In the Tungsten King mine, Arizona, beryl occurs in a scheelite-bearing vein. However, scheelite veins in Ne- vada and California sampled during the present inves- tigation contain little or no beryllium; this indicates that beryllium and tungsten are not invariably asso- ciated. Beryl occurs early in the mineral sequence in the few instances where it has been studied. At the Victorio Mountains, N. Mex., deposits, it forms a selvage on the 35 walls; and at Mount Antero, Colo., and Irish Creek, Va., it immediately follows the formation of some of the quartz. In a few places, as at Hill City, S. Dak., and Irish Creek, Va., the beryl-bearing quartz veins contain cassiterite instead of tungsten minerals. Stu- dies of foreign deposits (Tetyaev, 1918; Turner, 1919) where both tin and tungsten occur in the veins indicate that cassiterite may be later in the mineral sequence than tungsten minerals At Irish Creek, cassiterite and beryl are nearly contemporaneous (Koschmann, Glass, and V hay, 1942, p. 280). The occurrence of beryllium in quartz veins contain- ing tin and tungsten suggests that it might also be ex- pected in molybdenum deposits. Molybdenite is a major constituent in a beryl-bearing vein at Mount An- tero, Colo., and at the Black Pearl mine, Yavapai County, Ariz., and the two minerals occur together in several veins in Asia. However, most of the molyb- denite deposits in the United States that have been tested contain little beryllium, including those at Cli- max, Colo., Red River, N. Mex., and Bunker Hill, Ariz. Although the content of beryllium probably varies markedly throughout a given vein, as is true for tung- sten, it appears to average 0.0X percent BeQO for those tungsten veins in which beryllium is present. In two veins sampled in detail (Tungsten King mine, Little Dragoon district, Arizona, and Eloi claim, Victorio Mountains, New Mexico), there is no correlation be- tween tungsten and beryllium content, although most samples high in beryllium content also contained ap- preciable tungsten. The vein system at the Tungsten King mine extends for several thousand feet but has been sampled for beryllium over only a small part of its length. Some veinlike bodies that are otherwise similar to those described above contain feldspar (Norman, 1945; Carne, 1911, p. 58, 67) and are probably transitional be- tween the quartz-tungsten-beryllium veins and quartz- rich parts of pegmatites. Several of the quartz-tung- sten-beryllium veins appear to be related to neighbor- ing pegmatites. @QUARTZ-GOLD VEINS Samples of gold ores from the epithermal veins in the Oatman district, Mohave County, Ariz., and the hypothermal veins in the Bald Mountain district, Lawrence County, S. Dak., contain about 0.01 percent BeO (see table 14). In both districts (Wilson, Cun- ningham, and Butler, 1934, p. 80-115; Connolly, 1927, p. 60-94) the gangue includes carbonates and fluorite. The beryllium-bearing mineral has not been deter- mined. 36 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TaBu® 14.-Beryllia in some veins and related deposits in the United States Number Percent BeO Locality of 1581111 Mineralogy * Principal metals High Low Average Victorio Mts., N. Mex.: Eloi-Morloch claims..__.. 7 0.02 0. 005 0.02 Quartz, beryl, muscovite, wolframite....._______ w. Mount Antero, Chaffee County, Colo.: California BI Neuron seee needa . . 016 Quartz, beryl, molybdenite..........____________ Mo. mine. Providence Mts., San Bernardino County, Calif.: 2 .01 . 01 5.01 Sohoellfo, qHAFL3. . ... 00. ...n 0.1 ... cece w. Scheelite Ray mine. Little Dragoon Mts., Cochise County, Ariz.: 4 . 052 . 0008 . 01 Quartz, scheelite, beryl, chlorite.....__._____.__._ % Tungsten King mine. San Francisco district, Mohave County, Ariz_.__. 467 .03 T <. 001 (3) 5.0L Quartz, calcite, orthoclase, gold, fluorite....____. Au. Bald Mtn. district, Lawrence County, S. Dak... 44 .02 . 01 8.01 Quartz, dolomite, glauconite, pyrite, gold, ar- | Au. senopyrite, sylvanite, fluorite. Thomas Range, Juab County, Utah: Bell Hill I (enones tne nee 5.00X | Fluorite, clay, hematite, calcite. ..._._______.___ F. mine. Vance County, N. C.: Hamme mine....._______.. 163 . 008 . 004 8.007 Quarts, 2. w. Warren and Lyman, Grafton County, N. H...___ 42 . 006 . 006 8.006 Sphalerite, :.. Zn, Pb. Apache district, Sierra County, N. Mex.: Mid- 2 .01 <. 0004 5.005 Quartz, bornite, garnet, epidote_.......___..___. Cu. night mine. Red River, Taos County, N. Mex.: Questa mine.. 5 . 004 . 0005 . 004 Quartz, calcite, molybdenite..._._______________ Mo. Butte district, Silver Bow County, Mont_...._... 8 . 007 . 0005 . 003 Galena, sphalerite, rhodonite, rhodochrosite, | Pb, Zn. pyrite, helvite. Black Range, Catron County, N. Mex.: Taylor a arta loon ipa 5.002 Oageiforite . 22.3.2. 00 ELLs 0s. cou eee oie an Sn. Creek mine. Burro Mts., Grant County, N. Mex.: Long Lost Til rsn aeon lance re 8.002 Fluorite, manganese oxides. ........_____._____.__ F. Brother claim. Creede district, Mineral County, Colo_.____...._. 2 .002 .002 8.002 Amethyst, galena, sphalerite_..___....._________ Ag, Au, Pb, Zn. Terlingua district, Brewster County, Tex. 44 .005 <.001(3) 5.002 Cinnabar, calcite, gypsum, pyrite.... Hg. Holden, Chelan County, Wash.._._.. e +63 . 001 7.001(1) 8 . 001 Chalcopyrite, pyrite, sphalerite. . ___.... Cu, Zn, Au. Sundance area, Crook County, Wyo.........._.__ 2 . O0X . 000 X 8 . O01 Fluorite, quartz, calcite, limonite_...___________._ ¥. Mother Lode district, Eldorado, Calaveras, and 4623 . 002 <. 001 8 . O01 Quartz, gold, ferrodolomite, sericite, albite, | Au. Amador Counties, Calif. pyrite. Little Dragoon Mts., Cochise County, Ariz.: Blue- 83 . 0019 . 0005 . O01 Quartz, muscovite ("'greisen""), huebnerite, | W. bird mine. scheelite, fluorite, beryl. Encampment district, Carbon County, Wyo.... 2 .002 <. 0001 . O01 Chalcopyrite, pyrite, bornite, covellite, siderite, | Cu. 5 quartz, malachite, azurite. Silver Crown district, Laramie County, Wyo.... 2 <. 001 <. 001 <. 001 Chalcopyrite, quartz, azurite, malachite, pyrite, | Cu. limonite. Juneau, Alaska: Alaska-JTuneau mine......._.._._. M seer ece e eevee 5 <. 001 Quartz, calcite, rutile, tourmaline, pyrite, gold..| Au, Ag, Pb. Metaline district, Pend Oreille County, Wash.... 428 <. 001 <. 001 5 <. 001 Spbalerite; .:. Zn, Pb. Northport district, Stevens County, Wash.: Van A THat edo 5 <. 001 Galena, sphalerite, tetrahedrite....______________ Zn, Pb. Stone mine. Republic district, Ferry County, Wash.: Knob AT Aso lec evo 5 <. 001 Quartz, tetrahedrite, pyrite, chalcopyrite._._____ Au. Hill mine. Mehama, Marion County, Ore._.___..____________ 43 <. 001 <. 001 5 <. 001 ee aeon o 2 e ue een se dere awe coe Zn. Glen County, Calif.: Gray Eagle mine..._.__._.___ 45 | <.o01 <. 001 5 <. 001 Cr. Guernerville, Sonoma County, Calif.: Mount 162 <. 001 <. 001 5 <. 001 Chalcedony, cinnabar, pyrite. ......__..________ Hg. Jackson mine. San Luis Obispo County, Calif.: Costro mine. .._. 463 <. 001 <. 001 5 <. 001 - - eres ee neces s eon cer eens Cr. Rociada, San Miguel County, N. Mex.: Azure I (EH nn inn ee ull 5<.0004 | Quartz, garnet, epidote, bornite, hematite..____. Ca. Chief mine. Willow Creek, San Miguel County, N. Mex.: | [ece dunn poor 5<.0004 | Quartz, chlorite, actinolite, muscovite, tourma- | Zn, Pb. Pecos mine. line, pyrite, sphalerite, galena, chalcopyrite. Cherry Creek district, White Pine County, Nev... 10 . 0009 <. 0001 0003 | Quartz, feldspar, scheelite, sulfides._____________ w. Wauconda district, Okanagan County, Wash..._. 44 . 0003 <. 0001 $,0002 | Quarts, calcite, Au. Douglas County, Ore.: Bonanza mine....___._____ 43 . 0004 <. 0001 5.0002 | Cinnabar, pyrite, calcite, quartz....____________ Hg. Clark Fork district, Banner County, Idaho: 44 . 0003 <. 0001 5.0002 | Siderite, quartz, galena, tetrahedrite..._________ Pb. Whitedelf mine. Tincup district, Gunnison County, Colo.......__. 6 . 0013 <. 0001 0002 | Molybdenite, galena, sphalerite, huebnerite, | Mo, W, Au. quartz, pyrite. Gallinas district, Lincoln County, N. Mex.: Red SY (ee Neri ee. ol needy 0002 | Fluorite, barite, calcite, bastnaesite_....________ F. Cloud mine. Oroville district, Okanogan County, Wash........ 44 . 0002 <. 0001 5.0001 | Quartz, galena, chalcopyrite, pyrite, marcasite__| Pb, Cu. Marshall Lake district, Idaho County, Idaho.... 44 . 0004 <. 0001 0001 | Molybdenite, pyrite, galena, quartz_....___._.___ Au, Ag. Monarch district, Chaffee County, Colo.......... 3 . 0004 <. 0001 20000 "| mus O.. cre Jamestown district, Boulder County, Colo......__ - . 000 X <.000X 5.0001 | Fluorite, galena, sphalerite, tetrahedrite, quartz, | Pb, Zn. clay, pyrite, chalcopyrite. Beaverhead County, Mont.: Poison Lake mine... I ees nn eae eee ne aes 5 <.000X | Fluorite, thorite, monazite, pyrite, quartz, feld- | F. spar, calcite. St. Peters Dome district, El Paso County, Colo.: TM- -- «Toc fle 5 <.000X | Fluorite, galena, sphalerite, quartz, pyrite, clay, | F, Pb, Zn. Sheffield claim. kasolite. Querida area, Custer County, Colo...._...____._._. I ere dee eee ieee 000X | Pyrite, quartz, limonite, galena, sphalerite, | Ag. pyrargyrite. Mountain Pass, San Bernardino County, Calif.... 11 3 <.000X <.000X 5 <.000X | Calcite, barite, bastnaesite....._.....______..____ Ce, etc. Lake City district, Hinsdale County, Colo....._... 8 . 0002 " <. 0001 (6) <. 0001 Galena, sphalerite, rhodochrosite, quartz......_. Au, Ag. See footnotes at end of table. BERYLLIUM IN VEIN DEPOSITS TaBL® 14. -Beryllia in some veins and related deposits in the United States-Continued 37 Number Percent BeO Locality of fanlx- Mineralogy® Principal metals yl High Low Average Atolia district, San Bernardino County, Calif...... 8 | <0.0001 <0. 0001 <0.0001 | Quartz, scheelite, pyrite, calcite, stibnite_......~ w. White Pine County, Nev.: San Pedro mine...... $ <. 0001 <. 0001 <.0001 | Quartz, gold Au. % Basin district, Jefferson County, Mont....._...... 2 | <.0001 <. 0001 <.0001 | Galena, sphalerite, auriferous pyrite, chalcopy- | Cu, Au, Pb, Zn. rite, scheelite. Centennial district, Albany County, Wyo........ 2 <. 0001 <. 0001 <.0001 | Calcite, pyrite, garnet, sericite, limonite, quartz.] Au. Albany County, Wyo.: Rambler mine_..........~ 2 <. 0001 <. 0001 <.0001 | Covellite, azurite, malachite, quartz....._....... Cu, Pt. Montezuma district, Summit County, Colo....... 2 <. 0001 <. 0001 <.0001 | Galena, sphalerite, manganosiderite, rhodochro- | Ag, Pb, Zn. site, pyrite. Ophir district, San Miguel County, Colo.........~ I LRE l <.0001 | Galena, sphalerite, pyrite, wolframite, quartz, | Ag, Pb, Zn. tetrahedrite. Ouray district, Ouray County, Colo.._.._.......~ <.0001 | Galena, sphalerite, chalcopyrite, pyrite, thodo- | Ag, Pb, Zn. chrosite, dolomite. Platoro-Summitville district, Conejos County, <.0001 | Chalcopyrite, galena, sphalerite, quartz....._..~ Ag, Au. Colo. Poughkeepsie Gulch district, San Juan County, <.0001 | Quartz, galena, sphalerite, barite, tetrahedrite, | Au, Pb, Zn. Colo. rhodochrosite, rhodonite, pyrite. Upper Blue River area, Summit County, Colo.... <.0001 | Diopside, galena, sphalerite, molybdenite, py- | Au, Ag. rite, chalcopyrite, specularite. Upper Uncompahgre district, Ouray County, <.0001 | Galena, sphalerite, pyrite, fluorite, huebnerite, | Au, Pb, Zn. Colo. hematite, chalcopyrite, rhodochrosite. Wagon Wheel Gap, Mineral County, Colo........ <.0001 | Fluorite F. Congress, Yavapai County, Ariz.._______._._____.. 5 <. 001 Quartz, pyrite; SOLID Au. Globe district, Gila County, Ariz.: Castle Dome 5 <. 001 Quartz, pyrite, chalcopyrite, molybdenite, | Cu. mine. sphalerite, galena. Jerome, Yavapai County, Ariz.________.___.......- 5 <. 001 Quartz, dolomite, chlorite, pyrite, sphalerite, | Au, Cu. chalcopyrite. Mammoth, Pinal County, Ariz..._____.._____._...- 46 4 <. 001 1<.o01 (3) | s<.oo1 Quartz, orthoclase, sphalerite, galena, wulfenite, | Zn, Pb. vanadinite, fluorite. Pinal County, Ariz.: Childs-Alwinkle Mine.... 44 <. 001 <. 001 8 <. 001 Quartz, calcite, molybdenite, bornite, chalco- | Mo. Cu, Pb. pyrite. Vulture, Maricopa County, Ariz._._________.._.-- 47 <. 001 <. 001 8 <. 001 Quartz, pyrite, galena, sphalerite, gold..__...... Pb, Zn, Cu. Walker and Big Bug districts, Yavapai County, 125 <. 001 <. 001 5 <. 001 Quartz, calcite, pyrite, sphalerite, chalcopyrite, | Cu, Au,Ag. Ariz. galena. Wallapai district, Mohave County, Ariz..._...... 166 <. 001 1<.o01 (5) | s <.0o01 Quartz, pyrite, chalcopyrite, arsenopyrite, | Au. galena, molybdenite. Weaver and Black Rock districts, Yavapai 163 <. 001 <. 001 5 <. 001 Quartz, pyrite, galena, chalcopyrite........._... Au. County, Ariz. Pershing County, Nev.: Majuba Hill mine...... 123 <. 001 <. 001 5 <. 001 Cassiterite, chalcopyrite, pyrite, arsenopyrite, | Sn, Cu, Ag, U. quartz, tourmaline, fluorite. Pioche, Lincoln County, Nev........_..._........ APSA (elle AP- Ie 5 <. 001 Galena, sphalerite, pyrite, siderite...._..__._.... Au, Ag. Tintic, Ufabh County, Utab.....................«_ AMT I2. uci... <. 001 Quartz, barite, pyrite, galena, enargite.....__... Cu. Blackbird (and Nicholia) districts, Lemhi County, 4 4 <. 001 <. 001 5 <. 001 Quartz, siderite, pyrite, chalcopyrite, pyrrhotite, | Cu, Pb, Co. Idaho. galena, cobaltite, smaltite. Shoshone County, Idaho (three mines)..._........ 189 <. 001 1<.oo1 (6) | s<.oo1 Galena, sphalerite.........~ ( Zn, Pb, Ag. Warm Springs district, Blaine County, Idaho.... 44 <. 001 <. 001 5 <. 001 Quartz, galena, sphalerite, pyrite Zn, Pb. Judith Mts., Fergus County, Mont.: Spotted AH L_ 8 <. 001 OIG. 12... eL. che beanie Au. Horse mine. f Little Rockies district, Phillips County, Mont... 162 . 001 <. 001 5 <. 001 Quartz, muscovite, pyrite, gold, fluorite. .......~ Au. Stillwater County, Mont............._.__...-..... +8 <. 001 <. 001 8 <. 001 Chromite, Cr. Casper Mtn., Natrona County, Wyo. 2 <. 001 <. 001 <. 001 Albany County, Wyo.: Strong mine..._.......... THIEN |I sinema <. 001 Molybdenite, azurite, malachite, chalcopyrite, | Cu. tetrahedrite. Laramie County, Wyo.: Welcome mine........... A nls eae <. 001 un Fe. Boulder district, Boulder County, Colo....__..... £7 . 001 T<.001 (2) | 5 <.001 Quartz, ferberite, hematite, magnetite, fluorite..| W. Gold Hill, Boulder County, Colo.: Copper King 415 <. 001 <. 001 8 <. 001 Chalcopyrite, niccolite, pyrrhotite, pentlandite, | Cu, Ni. mine. pyrite. - Bonanza district, Saguache County, Colo......... 2 <. 001 <. 001 <. 001 Galena, sphalerite, rhodochrosite, zunyite, | Au. fluorite. Hillsboro district, Sierra County, N. Mex......... 422 <. 001 <. 001 8 <. 001 Quartz, pyrite, chalcopyrite, bornite, gold...... Cu. Lordsburg, Hidalgo County, N. Mex.: Bonney 162 <. 001 <. 001 5 <. 001 Quartz, muscovite, chlorite, pyrite, sphalerite, | Zn, Cu. mine. chalcopyrite. Shafter district, Presidio County, Tex.: Presidio AHA ALTA |: 5 <. 001 Dolomite, quartz, galena, sphalerite, argentite...| Ag, Pb, Au. mine. Tri-State district, Kansas and Oklahoma._...._.... 23 <. 001 <. 001 <. 001 Galena, sphalerite, marcasite, chert, barite... Pb, Zn. Keystone, Pennington County, S. Dak........... 415 . 01 <. 001 8 <. 001 Quartz, gold, arsenopyrite, ferrodolomite, | Au. biotite. Lead, Lawrence County, S. Dak.: Homestake 45 <. 001 <. 001 5 <. 001 Cummingtonite, biotite, quartz, carbonate, | Au. mine. arsenopyrite, pyrite, pyrrhotite, gold. Upper Mississippi Valley district, Lafayette and 46 <. 001 <. 001 5 <. 001 Calcite, marcasite, sphalerite, galena....._....... Zn, Pb. Iowa Counties, Wis. Rosiclaire, Hardin County, II1........__._........ 48 <. 001 1 <.001 (6) | 5 <.001 Calcite, fluorite, galena, sphalerite, pyrite....... Zn, Pb, F. Central Missouri district, Moniteau County, Mo. PSL [EAX dG 5 <. 001 Calcite, sphalerite, galena... Zn, Pb. See footnotes at end of table. 38 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TaBu® 14.-Beryllia in some veins and related deposits in the United States-Continued Number Percent BeO Locality of 1535111» Mineralogy * Principal metals is High Low Average Little Missouri R., Pike County, Ark._.__________ £16 | <0.001 <0. 001 5 <0. 001 (OUIADRE: 22. .c. 2. ool stb Hg. Alexander City, Tallapoosa, Als.: Hog Mtn. mine.. 412 <. 001 <. 001 5 <. 001 Quartz, chlorite, muscovite, gold...... ¥ Ducktown, Polk County, Tenn...._______________ 46 20 <. 001 <. 001 5 <. 001 Quartz, pyrrhotite, pyrite, chalcopyrite...__.... Cu, Fe. Goin, Clairborne County, Tenn.....__.__...___._.. 47 <. 001 <. 001 5 <. 001 Sphalerite, galena, calcite. .........._._.....__... Zn, Pb. Mascot, Knox County, 4166 <. 001 <. 001 8 <, 001 Dolomite, sphalerite, pyrite... -| Zn. Gratz, Owen County, Ky.... 46 <. 001 <. 001 5 <. 001 Sphalerite, galena, calcite. ._.......... -| Zn, Pb. Keweenaw region, Michigan........ 412 <. 001 <. 001 5 <. 001 Copper, epidote, quartz, calcite, adularia..______ Cu. Sanford Lake, Essex County, N. Y. R SSI (cl soo 5 <. 001 Timenite, Ti, Fe, V. Galax, Carroll County, 411 <. 001 <. 001 5 <. 001 Quartz, amphibole, biotite, pyrrhotite, chal- | Cu. copyrite. Virgilina, Halifax County, Va.: Red Bank mine... 5 <. 001 Quartz, hematite, Au. Spottsylvania County, Vs.: Valzinco mine...... 5 <. 001 Quartz, chlorite, pyrite, sphalerite, chalcopyrite, | Pb, Zn. galena. Allegheny County, N. C.;: Ore Knob mine........ 5 <. 001 Pyrrhotite, pyrite, chalcopyrite, quartz...._.._. Cu. Finley, Caldwell County, N. C.._.__..... M 5 <. 001 Iimenite, rutile, chlorite, tale....__...__.. Ti Union County, N. C.: Howie mine...._._...__._.. 5 <. 001 Quartz, biotite, chlorite, pyrite, gold.....__._... Au. Ag. Kershaw, Lancaster County, S. C.: Haile mine..... 5 <. 001 Quartz, muscovite, pyrite, gold, Au, Ag Orange County, Vt.: Elizabeth mine......_....... 5 <. 001 Quartz, feldspar, chalcopyrite, pyrrhotite. .._... Cu. Shelburne, Coos County, N. H......._............ CH (setae ci saol 8 8 <. 001 SDRAIGTIEG- (ccr 5111 eon inl Pb, Zn Marysvale, Piute County, Utah: Freedom No. 2 1 OOL S Tres? ence eus. 5 . 000 X Fluorite, pyrite, wad, uranophane, autunite, | U. claim. pitchblende. Red River, Taos County, N. Mex.: Chokecherry I il lle case cece ©0007. - | Fluorite, calcite, None Canyon. Elko County, Nev.: Good Hope mine__....._.... I ices +0007 -| BAHIfG .?. thre ees cons saas ees Ba. Climax, Lake County, Colo.: Climax mill. _...... 10 . 0006 . 0001 0006 | Quartz, molybdenite, pyrite, topaz, wolframite, | Mo, W chalcopyrite, cassiterite. Animas Forks district, San Juan County, Colo.... 12 . 0021 <. 0001 0006 | Rhodonite, galena, sphalerite, pyrite, quartz....| Au, Ag. Minerva district, White Pine County, Nev....... 5 . 0017 <. 0001 0006 | Quartz, calcite, scheelite_...._____._.________ + Bland district, Sandoval County, N. Mex.: Big 2 . 0007 . 0005 ©0000 -- | ~QUATVL, CACHO . , . . .- . cn Au. Sambo mine. Winfield district, Chaffee County, Colo........... 4 . 011 . 0001 0005 | Molybdenite, bismuthinite, pyrite, fluorite...... Mo, Bi, Au. Sacramento Pass district, White Pine County, hcg . 0008 <. 0001 0005 | Quartz, feldspar, scheelite, sulfides.._......._... w. Nev. Mineral Point district, San Juan County, Colo.... 4 . 0016 <. 0001 0004 | Galena, sphalerite, rhodonite, rhodochrosite, | Au, Hg. pyrite. Elizabethtown, Colfax County, N. Mex.; Baldy I {ase ceva dene t § <.0004 | Quartz, molybdenite, calcite........_______._.... Au, Mo. Deep mine. % Eureka, Grant County, N. Mex.: National and 4 <. 0004 <. 0004 5 <.0004 | Siderite, calcite, arsenopyrite, pyrite.....__...._ WwW, Cu. American mine. Lordsburg, Hidalgo County, N. Mex.: Eighty- 3 <. 0004 <. 0004 § <.0004 | Quartz, muscovite, hematite, chalcopyrite, | Cu. five mine. tourmaline. 1 All samples collected during the present investigation by the U. S. Geological Survey, unless otherwise stated. 2 Mineral association in the vein, not necessarily related to time or origin. Listed in approximate order of abundance; known beryllium minerals in italics. 3 Samples collected by J. W. Adams, U. S. Geological Survey. + Samples collected by Mine, Mill, and Smelter Survey, U. S. Geological Survey. 5 Beryllium determinations on plates exposed for general scanning, not for quanti- tative beryllium determinations. A quartz vein cutting limestone at the Midnight mine in the Apache district, Sierra County, N. Mex., may be related to this type (Harley, 1934, p. 85). Ore from the vein, which contains gold and silver in ad- dition to bornite and other copper sulfides, was found to contain 0.01 percent BeQ. The few veins of this type that we sampled showed little or no beryllium and there is little indication that beryllium is at all common in quartz-gold veins. No veins of this type are reported to contain tungsten, although at Bald Mountain, S. Dak., tungsten deposits nearby are believed to be related in origin (Connolly, 1927, p. 95-97). 6 Mill concentrates or tailings only. " Number in parentheses indicates number of samples having BeO content below the limit of sensitivity. 8 Samples collected by J. R. Cooper, U. S. Geological Survey. * Samples collected by U. S. Bureau of Mines. !* Samples collected by J. C. Olson, U. S. Geological Survey. MANGANESE-LEAD-ZINC VEINS Originally described from Kapnik, Hungary (Szabo, 1882), beryllium-bearing veins of this type are found in the United States at the Sunnyside mine, Colorado (Burbank, 19832, p. 521), and Butte, Mont. (Hewett, 1937). Rhodonite, rhodochrosite, and other manganese minerals occur with quartz, helvite, and sulfides, with helvite last in the mineral sequence. From mineral associations and structure relations we infer that the manganese-helvite veins are of somewhat lower temperature than the tungsten-beryl veins. However, only veins that are rich in manganese contain BERYLLIUM IN HOT-SPRING DEPOSITS helvite, in which manganese is an essential constituent. We know of no vein deposit in which beryl and helvite are found. OTHER VEINS The helvite-bearing vugs and veins of the Carpenter district, Grant County, N. Mex., are probably similar to manganese-lead-zinc vein deposits; the helvite seems to have no genetic relation to silicate minerals. Some rhodonite was found in the Grandview mine, although not directly in association with the helvite. Fluorite, which is prevalent at the Grandview mine, is found also at the Sunnyside mine, Colorado, and at several of the mines in the Butte district, Montana. The veins in Colombia (Oppenheim, 1948), from which most of the world's emeralds are mined, are unique. Small fractures in limestones and shales are filled with calcite, dolomite, beryl, parasite, pyrite, quartz, and rarely barite and fluorite. BERYLLIUM IN HOT-SPRING DEPOSITS Beryllium has not been mentioned in the many de- tailed reports on the chemistry of volcanoes or those on the volcanic fumarole and hot-spring areas of Yel- lowstone and Katmai, but it may not have been specifi- cally looked for. Using enrichment procedures, Ku- roda (1939, 1940) was able to detect a maximum of about 0.000001 percent BeQ in waters of a large num- ber of the Japanese acid-sulfate hot springs. Beryl- lium was reported or its presence inferred in mineral springs studied by Mazade (1852), Bechamp (1866), and Fresenius (1933), but there is no indication of what proportion of these waters are juvenile. Detailed geochemical data given by Strock (1941b) indicate that the waters of Saratoga Springs-which contain more beryllium than yet measured in any other mineral water-are entirely meteoric, although the source of the beryllium itself is not postulated. Beryllium has been noted at several localities in - material deposited by hot springs. At Steamboat Springs, Nev., calcareous sinter and siliceous mud, both of recent origin and rich in pyrite and stibnite, con- tained 0.0002 to 0.0008 percent BeOQ (Brannock, and others, 1948, p. 224). Ferruginous and calcareous ma- terial from two hot springs in Sandoval County, N. Mex., contained less than 0.0005 percent BeQ, except for one sample of ferruginous material that contained 0.00X percent.* Sediments in a carbonate mineral spring in Germany were found to contain 0.0016 percent BeO (Rezek and Tomic, 1942). None of these deposits represent appreciable enrichment over the average + Analyses by A. T. Myers, U. S. Geological Survey, of material col- lected by C. S. Ross. 39 beryllium content of the crust; in particular the Be to Al ratio has not increased. During the present investigation samples were taken from three tufa deposits that were presumably formed by hot springs no longer active. Data for these samples are tabulated below : BeO Location Material (percent)! Golconda, Humboldt Manganese-iron-tungsten- 0. 016 County, Nev. rich tufa. Calcareous tufa (overly- <. 0001 ing above-mentioned tufa). Sogfwille, Mineral County, - Manganese-tungsten ore. . 007 ev. Cove Creek, Hot Springs Tufa_____.__----------- . 008 County, Ark. Ouray, Ouray County, Colo. ____do____------------ . 08 1 Analyses by U. S. Geological Survey. The relatively large amount of BeO in the material from Golconda, Nev., presumably is due to deposition of beryllium with the manganese, iron, and tungsten. The beryllium mineral in the deposit is not known; but as the tungsten has been adsorbed in amounts of as much as 6 percent in very fine grained masses of cryptomelane and psilomelane without forming minerals of its own (Kerr, 1946a, p. 78-79; 1940, p. 1377-1387), the beryl- lium may have been similarly adsorbed. Shallow veins are associated with the tufa deposits, and a very close connection between hot springs, fumarolic, and epither- mal deposits seems well established. Deposits similar to those at Golconda are quite rare, and by analogy, the similar and much lower grade beryllium deposits cannot be expected to be important as a source of beryl- lium. If the beryllium is adsorbed in the manganese minerals, the recovery problems would be even greater than they are for tungsten. Though of doubtful commercial value, the deposit of Golconda may provide important information regard- ing the origin of beryllium in hot springs. Scheelite de- posits occur in the vicinity of Golconda, and Kerr points out that underlying scheelite or wolframite veins may possibly have been the source of tungsten in the spring waters. In line with this reasoning, beryl-bearing tungsten veins or helvite-bearing tactites conceivably may have furnished beryllium. The scheelite deposits of this region probably are related to Cretaceous intru- sive rocks, whereas the hot-spring deposits are thought to be of Pleistocene age. The thermal waters may have leached tungsten and beryllium from the earlier deep- seated deposits and carried these elements to the sur- face. Beryllium-bearing hot springs may thus serve as a guide to deposits of relatively high beryllium content at depth. Sampling of all tactites and high-tempera- ture veins in the vicinity of such springs seems war- ranted. 40 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS A large proportion of the samples analyzed for beryl- lium in the present investigation were also analyzed spectrographically for other elements. All samples analyzed are included, whether or not they contained any beryllium. The data are compiled in table 15, by States, districts, and sample number. Many other spectrographic analyses for beryllium are in the files of the U. S. Geological Survey, most having been made during World War II in the countrywide sampling of mine, mill, and smelter products. The spectrographic data for those samples that showed more than 0.001 percent BeQO are given in table 16. The analyses that showed 0.001 percent BeQ or less have been summarized in tables 8, 10, 11, 13, and 14. The localities sampled are shown in figure 2. The older analyses of table 16 may be of a lower order of accuracy than those of table 15. Reanalysis for beryllium of several of the older samples indicates that the earlier determinations may be high by a factor of as much as four. Resampling at some localities also suggests that some of the older samples may have been contaminated in an unknown fashion with as much as 0.2 percent BeOQ. However, reanalyses of samples of tactite from Nevada were in agreement with earlier results. The reliability of determinations for elements other than beryllium has not been tested, but inaccuracies may have been introduced by contamination in grinding. Most of the samples were processed in a routine man- ner by commercial crushing and grinding equipment. Sandell (1947) has shown that even when reasonable precautions are taken by hand grinding in a Plattner mortar, as much as 0.028 percent iron is added to quartz and feldspar. Recent tests conducted by Myers and Barnett (1953) of the U. S. Geological Survey with standard grinding equipment showed additions of as much as 1.5 percent iron and 0.1 percent manganese in routine processing of these minerals. Correlations between beryllium and other elements are not apparent from the data provided in the tables. Unfortunately, the list of elements for which spectro- graphic determinations are available does not include some of those most likely to be correlated with beryl- lium. In igneous and metamorphic rocks, for exam- ple, two of the elements most important in determining the mineralogy are silicon and aluminum, and few de- terminations of these have been made in samples tested for beryllium. Analyses for fluorine, with which a cor- relation might be expected, are also lacking. Gravi- metric analyses for tungsten of samples from the Little Dragoon Mountains, Ariz., and Victorio Mountains, N. Mex., showed no significant relation to beryllium de- terminations. Some correlation between beryllium and zirconium was noted in the feldspathoidal rocks of the Raton volcanic region, New Mexico, and the Trans- Pecos Region of New Mexico and Texas. Geochemical relations between beryllium and certain other elements, particularly tin, tungsten, and fluorine, are suggested by the mineral associations noted in beryl- lium occurrences in veins and pyrometasomatic deposits (see tables 13 and 14), although they are not without exceptions. The apparent association of beryllium and fluorine is particularly striking. Fluorite occurs in two- thirds of all the beryl-bearing quartz veins so far re- ported throughout the world and in most of the helvite- bearing veins and pyrometasomatic deposits. Idocrase where associated with helvite contains abnormal amounts of fluorine as well as beryllium. The average fluorine content of igneous rocks is 0.04 percent in gab- bro, 0.085 percent in granite, and 0.103 percent in nepheline syenite (Koritnig, 1951, p. 111). These fig- ures show an approximate straight-line correlation with the corresponding averages for beryllia, there being ap- proximately 30 times as much fluorine as beryllia in igneous rocks, plus an additional 0.03 percent fluorine. Lindgren (1983, p. 179) postulated a relation between fluorite distribution and magmatic differentiation in the western United States. He noted that intrusive rocks of intermediate composition near the Pacific Coast are succeeded by silicic intrusive rocks farther east, and finally by a belt of alkalic intrusives along the Rocky Mountain front. Fluorite is most abundant in the rocks and mineral deposits along the eastern mar- gin of the Rocky Mountains, particularly in the southern part. A corresponding concentration of beryllium in this zone might be expected because of the association of fluorine and beryllium in igneous rocks and mineral deposits. While the beryllium-bearing deposits of Iron Mountain and the Victorio Mountains, N. Mex., may be cited in support of this thesis, the virtual absence of beryllium elsewhere along the Rocky Mountain front and its presence in tactite deposits in Nevada and Cal- ifornia are opposed. Although the fluorite deposits of the Southern Rocky Mountains are believed to have a genetic relation to intruded igneous bodies nearby (Rothrock, Johnson, and Hahn, 1946, p. 21), the min- eralogy of many of them suggests a relatively low tem- perature origin that would not be favorable for depo- sition of beryllium. ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 41 EXPLANATION X20 Locality of sample ®10 Locality with analysis greater than 0.005 percent beryllia go owo 2.-Index map of localities listed in table 16. Alabama . Bakerhill lignite . Rock Run district, Emerson mine Arizona . San Francisco district Arkansas . Batesville . Fletcher mine . Glenwood district St. Joe district California . Elsinore lignite . Mother Lode district 10. Providence Mountains district, Scheelite Ray mine 11. 12. 13. 14. 15. 16. 17. 18. Georgia Cave Springs district, Callahan mine Cartersville district Michigan Houghton district Missouri Rocky Creek mine Nevada Tem Piute district New Hampshire Grafton County lead-zinc mines Ore Hill mine North Carolina Hamme mine 19. m Maitland district 22. 28. 24. 25. 26. . Southwest Virginia district, Glade Moun- South Dakota Keystone district Trojan and Lead districts Tennessee Bumpass Cove district, Embree mine Central Tennessee black shales Texas Terlingua district Utah South Temple Mountain Virginia Appalachian district tain mine OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 15.-Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; C, A. A. Chodos. nd, not determined; leaders (....) looked Ana- f Locality and sample lyst | BeO Sb | As Ba Bi B Cd CaO Cr Co Cu Ga Ge | In FeO; ARIZONA (see fig. 21) Cochise County: Courtland-Gleeson district: cr 0. 00X X0 0.00X |0.000X| 0.0X |0.00X |...... nd 3-6 PA rove . O0 X 6-10 |.00X | .O0X | X.0 »O0X [2.:. nd| X0 ¥ 19.04 |.......:.... .O0X X0 .0O0X | .O0X OX 400K [...... nd 3-6 F »007 {sss 00K XO :- (.cc. .000X| . OX | .00X |..____ nd 3-6 F . 004 . 000 X 6-10 .O0OX | . OOX ~O0X | :OOX |...... nd 6-10 F.] "| .000%) . 6-10 | .00X | .OX +K | 00K nd| _ 6-10 Little Dragoon Mts.: 820-449._..._._. F 20007 812: 1221200090 . OX 3-5 00X | .O0X .X OX |....s; nd 3-6 F i%. . OX 6-10 .O0X | .O0X SK 00x |...... nd 3-6 F 20007 |- xc cl -f: .-. . OX 6-10 O0X | .OOX . OX 00OX [.... nd 3-6 F ©1007 {-s sel . OX 1-3 «00X . MOX nd 1-3 320-539.._... 3-6 .O0X | . OOX aon nd 1-3 540... X0 OOK OX I .00X 1...;.. nd 1-3 544... X0 NOX... .oo OX 1;:00X |....«< nd 1-3 BHO: c..: X0 .O0X | . O0X «0X1 200X |...... nd 1-3 Pima County: Empire district: L. ce.. coc X0 . O0X 000X|...... nd 1-3 Bab. n ee cies X0 . O0X #0X |...... nd X0 $20.1 -contherkc« shat X0 . O0 X O00X|- ...-. nd X0 Parner ia ere evie ece X0 . O0X 00X |...... nd| X0 Helvetia district: nece nnn X0 . O0 X .000X|...... nd 3-6 nacre 6-10 . O0X nd 3-6 o [ (Mop oe t 6-10 . OOX nd 3-6 §15.ze.-. X0 . 000 X nd 3-6 SG 6-10 . O0X nd 3-6 Alf 6-10 . O0 X nd 3-6 520. 6-10 . O0 X nd| X0 eevente 6-10 . O0X nd| X0 Bas. en 6-10 . O0X 000X| .00X| - nd 3-6 Pima County: Pima district: 320-490... ¥ . 000 X X0 .OX | .00X nd| X0 Po cree. L .O0X 6-10 . X nd| X0 F -|- Re IA .O0X 6-10 .000X| . O0X . X A nd| X0 F . O01 .O0X 6-10 .O0OX | .000X| .00X | .00X |...... nd 3-6 F . 001 . O0X 6-10 . X »00K ..:... nd| X0 (P MEL eevee lc leat ed .O0X. 6-10 000 X| . 000X 0OX | . O0X nd 3-6 F X0 00OXL....«. OX" | 00K J:. ::. nd| X0 F X0 «OOK 1...-««« .O0OX | .00X - nd 3-6 F . 3-0. 6) .000X]._..... OOXML nd 1-3 F . 3-0. 6] .000X|].._.... OOK (Aras ens nd 1-3 F 6-10 000X |.... .... .O0OX | .O0X | .OX nd| X0 F X0 +O0K {-se .O0X | .00X | .00X| nd| X0 F 6-10 .O0X | .O0X «R | nd 3-6 F 6-10 .O0X | .O0X TK 1 cles nd 3-6 Santa Cruz County: Patagonia district: L1 lol eve F X0 .000X| . O0X w d nd| X0 6-10 .00X | .00X | X nd| X0 6-10 .O0X | .00X .OX nd 3-6 ¢ X0 OOK |-.1 :%... . OX nd| X0 ;00X 10% |...... .OX 6-10 .O0X | .O0X K nd 3-6 »OOX | ].. s . X0 .O0X | . O0X > 4 nd| X0 .O0OX | . O0X 6-10 .O0OX | .000X| . OX nd| X0 .OOX | .00X 6-10 .O0OX | .000X OX nd 6-10 OOR [ene 6-10 .000X| . 00X .OX nd| X0 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 4 3 elements in samples analyzed for beryllium for but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent]. La Pb MgO Mn Mo Ni Nb Ag NazO Sr Ta Sn Ti w U eU |eU;0s| V ¥ Zn Zr X ...as 0. 00X 0. 3-0. 6 $.X |.. .... nd. $. % |...... nd| 0.001 nd|0.00X |....--- 0. X | 0.0X 9 L/. 000 X. .3-0.6 X 1.2 21 00K |.. as.. nd nd| .O0X |......[......« PX see nd| _ .001 nd! .00X |...... .OX| .OX 3 .1-0.3 | X 0.00X| .O0X |....-- 0. OOX nd| . 4 . 1-0. 3 . X .00X| .O0X |...... . 000 X nd| . 5 .3-0.6 «K «se nd| . 6 .6-1 GK cess [se... . 000X. nd| . M 6-1 JX .00X| .000X|...... . 000 X nd| . $ 6-1 . X .00X| .O00X)...... .000 X nd] . O 6-1 -X .O0X| .000X|]...... . 000 X nd| . 10 wee . 3-0. 6 . X OOK |. -.». {.c.c--es nd| . . 03-0. 06) X0 nd| . 1-0.3 OX nd 1-0.3 OX nd| . 1-0.3 OX nd| . 16 [#.. izes 000 X 6-1. 0 . X nd| . 10 1-0.3 -K nd| . 17 |i-sses 000 X 3-0. 6 «X nd| . 18 00X 1-0.3 -X nd| . . 6-1 s0OX |...<-< .000 X nd| . 64 »A OX J .O0X .O0OX nd| . 3-6 -X ;00X|-.O0X |....» . 000 X nd| . 6-1 +X .00X| .O0X |...... . 000 X nd| . 6-1 . X ;O0X].00X |...... .O0OX nd] . . 3-0. 6 ed ~O0OX[ 00K |.----. . 000 X nd| . 6-1 CK Gla OX |...... .O0X nd| . . 6-1 .X ~00X| O0OX . 000 X nd| . . 6-1 X 00X| ;O0X J...... .O0X nd| . .1- .3 -X nd| . . 1-0. 3 AK nd| . .6-1 is: nd 1-3 -K nd| . .3 . X nd| . .3 X nd| . . 1-0.3 ~X nd. 6-1 +X nd| . .X nd| . . X nd| . .X nd| . .X nd| . & 6-1 nd| . 6-1 nd| . 06-0. 1 X .O0X| .O0X |-....- .O0X nd| . 1-0.3 | X ;00X) .O0X |...«.. .OX nd| . .1-0.3 | X .O0X| .000X|.....- .000X nd| . 06-0. 1 o < O0X|400X {...-- O00 X nd| . £ + * s .1-0.3 | X OX [00K {...». .O0OX nd| . 90K | - +X nd| _ .001 X .O0X .1-0.3 ~x% .00X| .O0X |...... . 000 X nd| . .0X | .X nd| _ nd{-.00X |...... X OOX. 1-0.3 .X 00X| .O0X |....-- . 000 X nd| . i0X ndj......- ndl.OX +X |: 00x 1-0.3 | X .O0X] .O0X |...... .O0X nd| . a Kile sre ndi....... -X 1 .0X .03-0.06| . X .O0X| .00X |.....- 000 X nd| . .00X| .OX| nd| .001 nd|.O0X |...... X 00X OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TABLE 15.-Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; C, A. A. Chodos. nd, not determined; leaders (....) looke a- Locality and sample if!“ BeO Sb As Ba Bi B Cd CaO Cr Co - Cu Ga Ge In FeO; NEW MEXICO (see fig. 20) Catron County, Black Range district: MTM Lede nee cen F 0.002 : 00. 0: 00K | sac ees ece ease 0. 1-0. 3]0.00X |...... 0.00X |0.00X |...... nd 3-6 Colfax County: Cimarroncito district: 820-076......... F ) er 6-10 |...... .OX nd 6-10 377. ) (0.0K {.cn 6-10 .00X |0.00X | X nd| 10 378. nd| X0 382... nd| X0 Colfax County: Elizabethtown district: AA. F nd 1-3 F nd 1-3 F nd 6-10 F nd| X0 F nd| X0 F i f nd 3.0 F AL. cll te. 6-10 .O0X | . 00X 000 X] .00X |...... nd| X0 F OX -| nels 6-10 00X | .O0X |...._.... 00X |...... nd 3-6 Raton volcanic region: 820-000. us SOK reel reese le reese .O0X nd 1-3 .OX .O0X nd 1-3 . OX .O0X nd 1-3 .OX 00 X nd 1-3 .X .O0X nd 3-6 . OX 00X nd 1-3 BX 12s ele c cee -| .O0X [...... nd 3 OK [-AL cae lll OX | .00X |...... nd 1-3 Dona Ana County: | Organ district: f 320-790 ... F OX |.00X 6-10 00X | .OOX OX nd| X0 791. F .00X | . OX x0 000X| .000X1- .X . nd| X0 793... F OX (|. x0 O0X | .000X| .00X | .00X |...... nd 6-10 794... F .O0X | . OX ndi.....- KQ s 12...s .000X| _. X +O0X nd| X0 706....2... F |.0X Ad{-._:.. 6-10 00X | .000X OX |.00X |...... nd 1-3 F .O0X | .OX nd| 0. 0X §-10 |.....s. .OX AK a nd 3-6 7978. F .O0X | . OX 6-10 00X | .000X| . OX O0X |...... nd| X0 P (eee races cuses OX |.socll 610° |..-.:.. 00X . X 00X |...... nd 3-6 reece ¥ - |r reseed eres lac X 00K. | 222... 640 - inn OX ls nd 3-0. 6 Grant County: Burro Mountains: BRU MBI se e wes F 2002 re Eee cases. X0 . 000 X]... .... . O0X nd . 1-0. 3 $19... F 001 00x [...... |...: 6-10 00X | .O0X X nd 3-6 Carpenter district: $20 ccc F OL Ny re +00X | .OX [..;.... .OX 6 »00X >] .000X| --.OX nd 3-6 Central district: nd 3-6 nd 3 nd| X0 nd| X0 nd| X0 nd| X0 nd| X0 nd 1-3 nd| X nd| X0 nd| X0 nd 6-10 nd 1-3 nd 6-10 nd 1-3 nd . OX nd| X0 nd| X0 nd| X0 nd 1-3 nd| X0 nd 6-10 nd 3 nd 3-6 nd 3-6 nd, 3-6 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS elements in samples analyzed for beryllium-Continued for but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent]. 45 La Pb MgO Mn Mo Ni Nb Ag NaO Sr Ta Sn Ti eU |eUsOs Zr 0. 0X 0. 00 X 0. 0X 0. X 0.0X nd nd, nd, 0. 002 nd 0. 00X 0.0X|--...--- 46 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TaBu® 15.-Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; C, A. A. Chodos. nd, not determined; leaders (....) looked Ana- Locality and sample lyst | BeO Sb As Ba Bi B Cd CaO Cr Co Cu Ga Ge In FeO: NEW MEXICO-Continued Grant County-Continued Pinos Altos district: 110 §20-70B.2L . roos esen ¥ cree. 0.00X |0.0X |...... 0. OX 1-3 0.003 10.00% | ©0. X. . nd| X0 111 R= {ees 0.0X| .00X | .O0X|.___... .OX 3-6 . 000 X) . 000 X OK nd| X0 Hidalgo County: Apache No. 2 district: 112 Ae ® .OX nd 3-6 113 755... .O0X nd| X0 14 781... .O0X nd| X0 115 MS crede e ened .OX nd 3-6 Hidalgo County: Hachita district: 116 G2... .c elit u F nd 6-10 117 nd| X0 118 nd| X0 119 nd| X0 120 nd 1-3 121 nd 3-6 122 nd| X0 123 nd 3-6 124 nd 1-3 125 nd| X0 126 nd 1-3 127.]. |=" BRP AAL. LIL. "FB lsc ~ »00% | AOOX IO 00% I...: 2:1 -: seo. sl m .x nd 1-3 128.1 -, 1. 4" ARQ. co OP. c ste |ate carlacecesl. ec | 1. .-22.1" . 148 % 10008) 200081 - «Xx. nd 1-3 120 |. S eee e Ro (ede - [YK "Lirc "£040 ~I 20008 - OOx I % - sae. nd| X0 130 nene » OOXH OX clu cee... X0 .O0X | . 000X nd 3-6 131 429 ... -0X | xo .00X | . O0X nd| _ 3-6 132 ABM P do NOX {sie de x0 00X | . 000X nd| X0 Lincoln County: Capitan district: 133 BRO BID-. andin enone ® 10.005 |::--l.lc.l.l. OX SL.AZ. »00X |...:.: 846 1... csfo|ccelll. .000X] .00X |...... nd 1-3 Gallinas district: 134 BIN -BUB-. c F 2008-2... cl. »O0X | eee ens eee, P 000 X| .000X] .00X |...... nd| X0 Luna County: Tres Hermanas district: 135 320-759... Zel) P 00X |...... v X0 ;000X|....... OOX nd 3 136 F {e OOK 1. OX sice X0 ;O0X | 000X| : :O0X nd 1-3 Victorio Mountains: 137 20-000... 22200000000» denne F .02 00X |:...... OX 000X|0.00X| - nd 1-3 138 BOQ k F . 003 O0X |...... OOX |c«ooce. . O0 X nd 6-1 139 899......... F , 004 ©0OX|--...:: O0OX nd 3-0.6 140 F +4 000X| . OOX .0X |.000X) .00X| nd| X0 141 F .02 0©00X|....... OX nd 3-0. 6 142 F .2 00X |..::... .X nd| X0 143 F . 005 000X|-...... OOX I nd 6-1 144 F 002 000X]....... +O0OX [00K 1-3 145 F .03 00X | .000X| .0X | .000X| .OX |...... X0 146 F . 006 O0X OX | .O0X | OX |...... 6-10 147 F . 06 00X | .000X .00X | .00X | .OX |...... 3-6 148 F . 005 -.... | o 3-0. 6 149 F .02 000X|....... .O0X | .000X| .00X|...... 1-8 150 F . 005 O0X | .000X| .00X | .000X|-_____]._._... 1-3 151 F . 008 00X | .000X| .00X | .000X| .O0X|..._.. X0 152 F . 002 .000X| .OX 00X | .OX |...... X0 San Miguel County: Rociada district: 153 Se OEC. cei ceo F| cel »O0X |. ssg. O0X |.... 6-10 .00X | .00X | X .O0X X0 Willow Creek district: 154 B20 .cc .00X | .OX | .O0X | . OX .3-0. 6) .000X|-...... «OX T200X .se 3 Santa Fe County: New Placers district: 155 «OK 6-10 .00X | .00X | X . O0X 6-10 156 OX |.... X0 00X | .O0X 1-8 157 t...22. X0 TOX 3-6 158 <00%: |:: XJ. x0 sO0K |.: a.. 6-10 159 OX : |. iuge. X0 .O0X | . OX 3-6 160 HOK 6-10 .O0X | . O0X 3-6 161 OX [-As 6-10 .O0X | . 00X 3-6 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 47 elements in samples analyzed for berylltium-Continued for but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent] La Pb MgO Mn Mo Ni Nb Ag NazO0 Sr Ta Sn Ti W U eU |eU;,0s| V ¥ Zn Zr 1104._...... 0.0X 0. 1-0. 3 0. X 0.:00X |...... 0. O0X 0.0X |... -- nd| 0.001 X 0. 00X 111 X . 3-0. 6 x OX |...... .O0X nd| .O0X nd 001 {esis. X .O0X 6-1 2di0.00X . O0X MS -|. .6 nd . O01 nd x00X . O0OX .O0OX .3 nd| .00X |0.00X .OX| .O0X HST: 6 nd| _ .001 fid)-s00X . OOX .3-0.6 nd| - .006 .6 ndii...... . 6-1 Hdif.«...- .6-1 Nd:... 1-3 Hdi.----. . 1-0. 3 nd| .002 «6-1 nd| .002 3 nd| _ .001 1-3 nd| - .003 . 1-0. 3 nd| _ .001 3-6 nd| . 001 .1-0.3 OX | .00X| .O0X nd! 00X=|:.clclulllsls {K nd| . 001 nd! .00X |...... .0OX| .00X .6 iX .O0X| . OOX nd! OX | hue Nast nd| . 001 nd| .00X |-......- .OX| .00X «6-1 -X .00X| . O0X ndi - 0OX .OX | . OX nd| - .002 .OX| .00X $80°j......t X 1-3 OX |. MOX |. .. .- .O0X nd| . OX not .OX |...... .OX| .O0X 131 | 0.0X X 3 OX J: »OOX |.. 00X nd| .OX nd 002 nd| .O0X +X | -, 00X 199 (:...... 000X 3 OX [t «O0X |. ... O0 X nd| . OX j...... .OX| .00X 198 {s....l{s.._.i.k- 6-10 OX vies fd): O0X( ]. OK |.i.2.. nd nd, ndi... w. »OOX :.. ..+. .00X 194 | !. O0 Xi.: !...: 1-3 . OX | .00X| 200% |..._L.|._...s.. fd] OUX Verti nd nd nd! .0X | |...... .O0X 185 i co 1-3 .OX 0. O0X OX |...... ndi.-.=... nd| .00X | .O0X |...... .O0X 186 |_. .s «6 OX |.._.____] .00X - BOL ,OA O Xi As nd 001 nd| .O0X | .00X |-..---- 00X 6-10 X OX .OX 02 nd .O0X 6-10 X OX OK nd .O0X 6-10 .X G0X | AOX nd .O0X 1-3 X OX | .OX| nd .O0X X0 X ndi. . nd|.......] .OOX 1.....«..| ' «OR...... 1-3 . OX 00X | .OX 08 nd .O0X X0 X OX | :GOX|...... ndl.: «nd! 001} +00X .6-1 «X 90X | .OX |...... nd .O0X 3-6 X OX X .OX| nd .O0X 1-3 X .OX X . 04 nd. .O0X 3-6 X . OX .X . 06 nd .O0OX X0 -K 00X | .OX |...... nd, .O0X 1-3 >. « O0X | .O0X) .X nal: |...... .J -USORIC...... 1-3 < .00X | .O0X| .2 nol - nd{.......] .00X |.000X|® 3-6 -K O0X | |...... nd .O0X . 6-1 X OX K nd .OX 198 3-6 X 00X| .O0X |...... O0X nd{-.OX X: nd 001 Rd-OX . O0X 15¢ )...... X-xX0 . 1-0. 3 .X 00KI .GOX |... X Hdl. .-- .oo]. Vie. wens AOL eclsseetse X0 .00X .1-0.3 K nd| . iX |-cives nd| . 001 nd| . &6-1 .X nd| . KR H ease nd| .004 nd| . . 3-0. 6 X nd| . vRASil-onees nd| . 001 nd| . .1-0.3 -X nd| . -0K |...... nd| _ .001 nd| . .6-1 . X + nd| . sR S nd| _ .001 nd| . .O0X . 3-0. 6 in < .O0X| .O0X nd| . YC l nd| .003 nd| . .O0X . 1-0. 3 . X .O0X| . OOX nd| . JX nd| . 001 nd] . .O0X 48 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TaBu® 15.-Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; C, A. A. Chodos. nd, not determined; leaders (....) looked. Ana- Locality and sample lyst | BeO | Sb | As Ba Bi B Cd CaO Cr Co Cu Ga Ge | In FesOs NEW MEXICO-Continued Santa Fe County-Continued New Placers district-Continued 162 320-336..... F X0 0. O0X 3-6 163 F X0 .O0X 3-6 164 F X0 . OOX 6-10 165 F X0 .OOX X0 166 F 3-6 . OOX 1-3 167 3-6 .O0X 1-3 168 3-6 . 000 X 3-6 169 X0 . O0OX 3-6 170 p< .O0X 3-6 171 |. _._. al BDD ery U P Ue de ele +OK dL. lous 1-3 . 000 X. 1-3 Sierra County: Cuchillo Negro district: 172 3-6 00X | .OOX X nd 1-3 173 6-10 00X | .000X| .00X | .00X |...... nd 1-3 174 1-3 00X | . 00X . OX 00X |._icl. nd 3-6 175 3-6 OK nd 3 176 3-6 »00X .OX nd 1-3 TTL 3 +00. e neenee POT LOL . LE | OK less.. {cos}. 9s. 8-0. 6 ;:00X |...... e 4 nd «6-1 Socorro County, Jones Camp: 178 B20 BOU. Lec: cocco s FU [Even sOOX |.. rea ea el 3-6 .00X | . O0X OX - nd 3-6 TRANS-PECOS REGION (see pl. 1) Wind Mountain: KO _ [pessiQleuse... X.0 1-3 X0 X0 |...... &6-1 X0 + .3-0.6 IX nd, nd| .00X nd| nd| nd| *Major *Major nd nd| - .00X nd| nd| nd| *Major pR 000 X] .00X |...... nd| X X0 .OX | .00X .O0X | .00X nd| nd 1-3 X0 ...... £000X]...._:. nd| nd .1-0.3 1 O0X | .OX nd nd 1-3 1 OX |.lslle. O0X | .OX nd| nd 1-3 3-6 .O0X | . O0X X0 6-1 +00X |...... 3-6 3-6 .O0X | . 000X. 6-10 X0 +00X I....... 1-3 . 8-0. 6) .000X |...... 1-3 6-1 »O0X 3-6 6-10 .000X| . 00X 3-6 +40. 6, .0X |....._. 1-3 IK i X.0 1-3 . 000 X| . 000X 1-3 1-3 »OOX |...... 3-6 MONTANA (see fig. 67) Anaconda mill and smelter products: 201 BES Lele cl F .3-0.6 202 F . 1-0. 3) . 203 F 1-3 204 F . 6-1 205 F X0 206 F 3-6 207 F X0 208 F X0 209 F 3-0. 6 210 F 6-1 prbl F . 3-0. 6 212 F . 1-0. 3 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 49 elements in samples analyzed for beryllium—Cohtinued or but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent] La Pb MgO Mn Mo Ni | Nb Ag Naz0 Sr Ta Sn Ti w U eU |eUsOs| V ¥. Zn Zr nd{0.0X |..-c-.|.....c- 0. 0X nd, . OX nd .OX nd .OX nd, .X 167 nd +X 168 nd X 169 nd th€ 170 nd .X 171 nd .X 172 nd . OX 173 nd AX 174 nd .X 175 nd .OX O0 X. 176 ndi OX. X 177 not"; 00X OX 178 50 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TaBug® 15.-Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; C, A. A. Chodos. nd, not determined; leaders (....) looked Locality and sample fill-Is? BeO Sb As Ba Bi B Cd CaO Cr Co Cu Ga Ge In FeO; WYOMING (see fig. 46) Carbon County, Hanna district: 213 -L- coll}. oe M | 0.0003 nd| - nd nd| nd nd| - nd nd nd nd nd! 002 [...... nd nd Sweetwater County, Superior district: R 214 28-245. .cc.» - M . 0004 nd| nd nd| - nd nd| nd nd nd nd nd] .004 |__... nd, nd COLORADO (see fig. 49) Boulder County, Lafayette area: 215 T- ace- ec M nd| - nd nd| . nd nd| nd nd nd nd nd| . 004 nd nd 216 ares use aes . 0003 nd| - nd nd| - nd nd| nd nd nd nd nd] .003 nd nd Chaffee County: Monarch district: 217 $20-020. ece i000 neenee .. ¥ (Pe laa ul.... n. 0:000°%] .. 2212 2 . cns X0 0.00X |0.000X| 0.00X |0.00X |..___. nd| X0 218 021... F + X0 .O0OX | .000X| .00X | .O0X |___... nd| X0 Sedalia mine: 219 22-000 F 0004]. cece fine URK R ce cece cave ave X0 00% |...... .O0OX | .00X |__... nd 3-6 Conejos County: Platoro- Summitville district: 220 $29-5D4 .L. ..- .000X| . O0X .OX nd 1-3 221 595... .O0OX | .000X| . OX nd 3-6 222 B07. .O0X | .O0X iX nd 3-6 223 508. 000%)... .... .OX nd 3-6 Costilla County, La Veta area: 224 2s. cel cccebr enna nd nd nd|-.004 |...... nd nd Fremont County, Florence- Canon , City area: 225 nd nd nd] .004 nd nd 226 ITBs coo o nd nd nd| .004 nd nd Garfield County, Rifle- Silt area: j 227 SS- U8 nd nd nd! 004 |...... nd nd 228 nd nd nd} .005. |.!.... nd nd 220 nd nd nd] .005 |...... nd nd Gunnison County: Tron Hill: 210 ..: vec ene nd| X0 211 nd 10 212 nd| X0 213 nd| X0 214 nd 6-10 215 nd 3-6 216 nd| X0 217 nd| X0 218 nd| X0 219 nd| X0 220 nd nd 221 nd nd 222 nd nd 223 nd nd 224 nd nd 225 nd nd 226 nd nd 227 nd nd 228 nd 3-6 229 nd 3-6 230 3 s nd 3-6 281 000X] .00X | .00X | .O0X |...... nd| - 3-6 232 00X | .O0X OX nd 3-6 283 000X] . OOX O0X nd, 3-6 234 .O0X | . 00X .O0X nd 3-6 Italian Mountain: 235 329-002... . cee ne co aos ¥. {fe OX 1 |. 0.:0X |...... X0 OOK |.:...-< «00% |...... nd| X0 Snowmass Mountain: 236 cece cor renseck F 200. ss .cc]... 1000] Ave a[ -c ewes X0 .000X| . 00X .O0X | .000X]...... nd| X0 Tomichi district: 237 29099: F |. c. 3-6 .000X| . 00X nd| X0 238 023. d" £ |.. ...s X0 .00X | .000X nd, 1-3 2390 030 F. [S001 [..... :...... .O0X | .OX | .00% |...... 3-6 .O0X | . 00X nd| X0 Hinsdale County, Lake City district: $20 BTG. c. Lenee. coe ee abides PA nene C-- " {cece .O0X | .OX 3-0. 6) .000X|....... OX nd, 1-3 241 Fo c 9%" | OX ..:... .OX I X | | nd, 3-6 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS j 51 elements in samples analyzed for beryllium-Continued . for but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent] La Pb MgO Mn Mo Ni Nb Ag NasO Sr Ta Sn Ti w U eU |eUsOs| V ¥ Zn Zr 213 nd, nd nd nd nd nd| - nd nd nd nd! ~ndi....__. ' nd| nd| - nd|<0.001 nd|0. 02 nd nd| __ nd 214 nd, nd nd nd nd nd| - nd nd, nd ndi ndj....... na| nd| nd| <.001 nd| .008 nd nd nd 215 nd, nd, nd pd nd| _ nd| nd nd nal + 'nd| - nd|...---- nd| - nd| - nd| <.001 nd| . 01 nd nd, nd 216 nd nd nd nd nd nd| nd nd. nd nd! (nd.... nd| nd| nd| <.001 nd| . 01 nd, nd nd | g Mil Anise. 0. 00X 1-3 0.0K 0. X nd| nd nd nd| .O0X |0.00X | 0.0X| 0.00X 218 | 0.00X| .000X| 1-3 AOK (. an ness .X nd| nd nd nd| .OX | .O0X .OX| .00X 219 | .OX .O0X 6-10 'O0X ndl 20K) o < nd| - nd nd ndl .00X | .OX |....«.. .OX nd| _ nd HQI X . O0X nd| nd nd| .002| .OX | .00X |.....-- .OX nd| nd ndl -.002] «OX . OX nd| nd nd| < 002] .O0X |..._.._.|......~ .OX nd| - nd| <.001 nd| .0L nd nd rd nd| - nd| . 001 nd| . 007 nd nd nd nd| - nd 001 nd| . 001 nd nd nd nd| - nd| <. 001 nd| . 02 nd nd nd nd| - nd| _ .001 nd} . 01 nd nd nd nd| - nd| .002 nd| . 008 nd nd nd nd | nd . O0 X nd | nd . OX nd | nd . O0X nd | nd . OX nd | nd .OX nd | nd . OX nd | nd . OX nd | nd . OX nd |_ nd .X nd | nd . OX nd | nd . OX nd | nd .OX nd | nd . OX nd | nd . OX nd | nd . OX nd | nd .OX nd | nd . OX nd | nd . X nd| _ nd .OX nd| nd .X nd| _ nd . OX nd nd .OX nd nd . OX nd| nd .OX nd| nd O0X nd| nd nd, nd| . OX |...... 00X nd| - nd nd ndi .O0X |.......]......- .O0X 237 nd nd| nd 90K [ic.-.-- X . O0X 238 nd .X nd| - nd nd| .002] .OX | .OOX iX 1-..OX 239 nd . X nd| nd nd| .002] .OX | .O0X .0OX| .00X 240 ndi .X |._...Q[.-_...- SX nd| - nd nd| _ .002] .000X|...---- X . OOX 241 ROL .OX ndl nd ««« »O0X |...... X! {-.s..-- 52 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 15.-Spectrographic analyses, in percent, for other [Analysts, F. Janet D. Fletcher; M. K. J. Murata; C. A. A. Chodes. nd, not determined; leaders (....) looked Ana- Locality and sample lyst | BeOQ Sb As Ba Bi B Cd CaO Cr Co Cu Ga Ge In FeO; COLORADO-Continued Huerfano County, Walsenburg: 242 I... ede e deli ¥ 1 0:002 |.;...:|.._...l 6.0K 0. O0X 6-10 |0.0X |0.00X | 0.0X |0.00K |...... nd 3 248 | _ €. ] 0008 |......l......] .X .O0X 6-10 .OX | .00X ;O0X | .0O0X j...... nd 3 La Plata County, Durango area: f 244 cc coco noen ober ves besa M . 0003 nd| - nd nd| - nd nd| nd nd. nd nd nd| .004 10.006 nd nd 245 M ; 0006 nd| nd nd! nd nd| nd nd| __ nd nd nd| .005 | .007 nd nd 246 M [s... nd| nd nd| nd nd| nd nd nd nd nd! .004 |...... nd nd 247 M . 0003 nd| nd nd| nd nd| - nd nd nd nd 005 i...... nd nd 248 F sOX j..<.. 3-6 .OX |.00X «O0X { .00X |...... nd 3 249 F OX 00X |...... 3-6 OX | .000X | .O0X |...... nd 1-3 Mineral County, Creede district: 250 cen nee eee cel F 2008 +X | 00% 0. OX 1-0. 81 .000X|..._... ROX | al _ nd 1-3 251 eee ei cueveess F: [ 002 |...... .OX| .OX . 1-0. 3) .000X|....... +OX - nd 6-1 Park County, Tarryal district: 252 .0X [0M0O0XI.....__{._.... 6-10 .00X | . OX .OX nd| X0 253 DX (| X0 .OX 000X| . OX nd 3-6 254 OX Lucls. .O0X nd .1-0.3| .OX | .00X .O0X nd 3-6 255 DOX (eerie divine, nd| X0 +00X |.....s. .O0X nd nd Pitkin County, Redstone area: 256 ceo. eel M |*:0005 |...... nd nd| nd nd| nd nd nd nd nd{ .004' |..___. nd nd Summit County, Breckenridge dis- j trict: 257 828-0002. .. le he ® cgl... OX Afresseclel cued facade X0 .O0OX | .000X| .00X | .O0X |...... _ nd| X0 Tri-State lead-zine district: 258 328-325. sp ¥ |S +00X |.. «o.. nd X0 +00X J...... .OX nd . 3-0. 6 259 Sif ece on: s Pon [Ere er + 0OX |...... X0 +0OX |....... .O0X nd 3-0. 6 ARKANSAS Hot Springs County, Magnet Cove: 260 825-200. 0.00 ee oue F . 01 .OX .O0X X0 .OOX | .000X| _. - 3 261 F ' x0 262 F X0 263 F 1-3 Saline County: 264 cs sane.? C nd 265 843..__. C nd 266 $M. nent nere enn C nd NEW JERSEY Sussex County: Beemerville area: 267 nd 268 nd 260 nd 270 $ nd 271 .OX J..... _L... nd 272 278 274 NEW HAMPSHIRE Carroll County: Bartlett mine: 275 $20 c M ©0082 NOX) {-fr l PK L lenee re el e |- X.0 Red Hill area: 276 .ll elec ... C {000% cnc MOREL .O0KX [._.___J.__.... nd 277 BHS Hel cence O fe ece -.. OOK |e nsane s. nd| .000X|._._... ;000X| .GOX |....../...... _nd ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 53 elements in samples analyzed for beryllium-Continued for but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent] La Pb MgO Mn | Mo | Nt | Nb | ag | Nm6 | Sr | Ta | Sn | Fi | W | V | eU. feUsOs| V. J Zn | Zr 942 |:. 3-6 O UX 000K nQIO.OX TC \{ [seee nd| 0.001 0. 0X MD | 6-10 OX SOX nd| .X: X - nd| . 001 .OX 244 nd nd nd nd, nd, nd| nd nd, nd nd nd| nd| nd| .001 nd| . 02 nd nd nd 245 nd nd nd| _ nd nd nd| nd nd nd nd nd| nd| nd| <.001 nd| . 0L nd nd, nd 246 nd nd, nd nd nd nd| nd nd nd nd nd! nd| nd| <.001 nd| .006 nd nd, nd 247 nd nd nd nd nd nd| nd nd nd nd nd| nd| nd| .001 nd| . 008 nd, nd nd S 3-6 «OX OK - {ecs nd| OX |...... ndl...... .O0X nd| . 001 .O0X nd! ndi......- . O0X nd| nd 002 .O0X nd| - nd nd .OX nd| nd nd .OX nd| _ nd nd .OX nd| nd nd .O0X 256 nd nd. nd nd nd nd| - nd nd nd nd! nd| nd| nd| .001 nd| .02 nd, nd nd 257 | .00X| .000X| 1-3 VA OOX 9-4. | s00X |..._-.]Lazcus .X nd| _ nd| .002 nd| .00x [-....... .OX 958 [......s .OX nd ROJ »O0X . OX nd| - nd| .001 ndl.o0X |.00X | X. |....... 250 1..;.... . 000 X nd. ndl .00X| nd| nd nd, ndl.90% [.O0X | X _ |.._.... 260] OX |........« 1-3 Ao € Moree ;O0X [ .OX |...... nd| . OX tb d nd| nd nd, .OX 261 | .OX .000X| X0 «X ;00X|......- nd] . OX .OX nd nd nd . O0X 202 1-3 OX | 00K] .O0X nd| . OX WX nd nd nd, .OX 263 00X 000X| <.1 OX 00X| .O0X | .OX |._.....- ndl OX OX nd| nd nd .OX 264 | .OX . O0X hdl .. fndl.:...... nd| . OX ndl:...--- K cece. nd nd, b.d 265 | .OX .O0X nd| .X »OORL...c_.s nd| .OX ndj....... [| nd, nd -X 265 | .OX |.l...._.. ndl. Ke ndi... nd| .O0X ndi.s..... +X [ nd nd .X nd nd| .X nd nd -X nd, nd| . X nd nd .X nd, nd| .X nd nd, 4 nd nd| . OX nd nd . OX nd, nd| .X nd nd .OX KO : . .O0X ndj........ ndl,O0X OOK]... nd nd, .O0X nd| X 00X| . OOX nd| .00X nd| . OX ndl....... OX |...» nd nd, .O0X nd! x .O0X nd] .O0X nd| .OX OX... nd, nd .O0X 275 | .OX .O0X .OX 0B SJ ges nd! .000X|...-..]. ...... SK Pliceecs nd nd ndi....... «OX css.. . OX 276 | .00X|........- nd| SOK [.. c.--|-cacc-. nd{ .000X |........ .O0X ndl....... K nd, nd .OX 277 ndt AOX ndi..-.«.- nd| .O0X ndj....... K nd, nd .OX OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 54 ...... 10° ©00 bp ""~" 000 ° ("""" N* cole niin oo bpene aus £00 "1 SCS f ""opt ap "~"*~~**~ Mop '0g-LT6T ...... 10 (| $9 > [70 (p ria rms o(r (sr lass nl ligon plop ...... zo* | goo'> y o S mp E al "aT To T E T so wos |a cr (--- [-t- -=-4g "C>-986T ...... 10 (200 > (.~ ~ lsc oa ro ap re lente teese sf = toot (r= >--" rog 'ssute} prop |-~~~~~~t-p¥4v-gp f sor -StP opoT '&junop sopeuy ...... §0° .. | $00 > SOD [ "": r= 34 200° |~~~~~~] * |~~oreus tmo |-~~~--eare Ayuno opIsIOATY ...... £00 ° $00 100° 1-*~-*~| 100" |- go" |. . goo" une-nmiga ...................................................... 200 '0| _ ====~-[~~~~~~] 200° ogy |~~~~oupua *10pstp c0f "1g Aomag £" 10°. o e reer {noc tas $0 °0} ~*~" $00.1: P0 Is cc pahwine wite $00 5:18 o10 ouyneg |~~~~~ ourur s :Ayunop oureg 'sSuf 90° 20° 800 :> (1 31 (bf ptahoss £5.41 900° (Lie CIL (Ans tt con of frt es BOLI Hast T0 ' [18] osoussuepy |~~~~~~~~~~~ 9p. . VI 'se1u00 "ouput T 90 ° $00 > {.* *.~"~" . ars abot ubcict 8° 0 :* "e Can nap "Bie C {3 If" $00 0," ~~~** 800 * +09 osoussuepy UsopOuy |~==~~~~~~ T-XXV-HI ©19LI}STP pOOA ~uop 'Ajunop *o1o esouss &l 1" £00 > sole T Y E1 $0 (. as apa" £00" |"" ~""" pri a hle" TQ ' | ~usut |~~~~~~~~~~~~ . cabins porn ve "oud ~x0038 'slo}o pus 'q-I '00g 80° 6° £00 > |:" 90% : 0 t" | oT f [=r ees $01. Cop ffir jo 1 op ~* "189DILM 'If IIE |~~~~~~~~ € > ~x0038 pus 1: E! ©00 > 1:5 80 %4"~*~~> 100 101 ~*" "~ ESL: $0 ° (*f nino 800 '0):":*~: B0 e aon santos tof I3 op?" |~~~~~- ve 'ordures 'o1o asouss qe1s ortdxoo3s 90 ° 8° £00 '> |--: so ap rl eres 1" 1. $0. 050 Aen t c" ©00 "01 90 "ATE I0° | -ustopei2-4@y | 'oupur |--~~~~~- E-MXHV-HT of[fasoreg '&yunop f ...... 20° 800 t> .[; ala ~ NEST C20] 200 " | 800 A00 G00 * "TOD ~- "7 | "*~ "ound |-" ~*~ ~ 6 SLT # 'werqery 'orupt ...... 10° B00 (>> [FCA orer o [~|~=~~~~~~ idl iC (obra 80 * -|- 800 D| ~: *= "("f 80° | - osoue8uepy uossours; |~~~~~=~~~~-- T-d-€I mommstp uny xoog '&junop it-OT-6f , oAtp ut 4; gregg | coutustt (IIH Joxeg ...... PDs (CNC mep fronton tso -=- Lmao tol" "1 ~~~ ~*s[- ap 200 '0|~~~~~~4spo ontusr7 | sg0g | '414unop imogqisg ©O4Z | "OFA 'no f'OM | ous |'OWL ['O'LL 'O'4N| ON |fOOWt| OSH 'o'*T| 'o'] oop [top| oop | OPD | '0'd |:otas| 0d ordurss Jo co mog qrdures pus [pogou ordures 107 4dooxe 'qrqqey 'o ugor qs4peuy] haaing morbojoap *g 'r) ay; fo sopf ay; wouf 'quaousd us 'soshzpun orydviboupads #1gavy1, 55 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 10° A. 10° 100 ° 20 ° 33 10 ° 10° 10 ° 10 ° sseessesssssssssssssss f e s i! $0" !" zoo | goo 'ol 10° |~~~~~~ £0 ° so [ffs calc cua typ 100 ' Ixd to :| "~~" £00 -: 'A 200 ° 10° ISi [~~~ at Wop £00 ° 10° $00 ° 80" $00 {:~ "~~. "" $00 ° -| 300+ [==--] 10° £: ........ go n [<--- 10° ........ $0 [*:* : Sop T Hl ""~" $0} 20 ° 100 -- "]" "~ 2" 20 ° ........ o" 00 "0"! 'S" i so" ........ go "H" 100 I| 480° £0 ° AT $0. ........ go> ........ ©0 " A00" (~" ""J 90° ........ 20" | "***" 100 1 aco ........ so i 100 (;- Yo" ........ 10 nl 20° ........ 800 |~*~~*=| 100 " co" 800 ° 100 ' 20 ° ........ 800 * 100 ° |~ 20° ........ $00; | 100 ""~" 80° 800 . is (idl attain 10° ........ 10 { 100" _ 60" |||||||| to" |**~5~s{ $00 |"" "f( 60" 20 ° 100 Ns" "SB CCF 20 ° 20° 100 ° 20° ........ goo + |~=~~~~|~ 20 ........ goo : _ zo* oc #0 P )+ oll planer; soulers £00 61° $00 4 J: rss SE rT ICOC £00 ° ....................................... 10 .......................... ==-- ro ....................................... $00 ° .............. Jis ---!-------l ro" ....................................... 800 ° 20 ° 20 ° 20 ° 200 10° £00 ' 90 ° *arq©7 Jo puo 12 92g 90° k 100 ® 100 ' 100 * 100 * 100 ® $00 ° $: s 100 4 ["~ 9u00 |~~~~~~~~~~~~~ .o snape ya 100 [ 20% ([AP 10 ° ©f@040§ |~~~~~~~~~~~ \o (+4 90 ° OIS =I 1 O6 . Cpls wisi ataintstnnmenns op: "[[ ~" fd 1800 ODU 90 ° \| be 5C 200° | -Ins pus ognIg-t9,p |~~~~~~ 0G-MDGC-6¢ '10L9Sfp jnIJ-woJ, '&junop UOOUpT :SpBAON .............. 80° | so |~~~-a10 esouesuepy |- yooup £x00¥ 'Ajunopy uouusyg fmosstpt "9,81, 000 ¢ ...... 100° _ |-~-~~~| goo: | -uoo #if soddop |~*~~~-oupur Aoum® |--~~~~~~g-Inb-g1t seddop 'q0111stp uojq2nog .................... 50 " [*~~~******~~=op" ~*~ usUublfeO | ~~~". .~" 9 6-0-6 orustp ssupdg gasp 'Ajunoy .................... 10° plovJorieg | ~~~" ~~~" ................... 10° |~~=~~~~~~~~~-op-~~~~|oupur uiie |~~~~~~~~~$-g-Ad-94 tenet toh £00 1 "Cas Pac 2 \o newt ares, ne lm 54 9 .............. 900 * op ~- ~ ourur .................... 900 ® |=======~~~~=zop-~~~~|~-@uzur @8py¥ Ong |~~ ~~~~~~~~~&-1g-94 .................... 10 ° Top ~~~f 0p: el" "Sl .................... 10° op."; ~- op" ~~ ~- 'fit .................... 10° 0p :~ 5°" op=~" ~~Of .................... TVET e - Ci Fund | - -.. .................... (19g eine , Shuy a .................... S00 "4 s: ropa |f" ato mep ol'" "~~~" "Ai f #00 ® |~ op ~~ oP ila YZ WL .................... 800" ooo fun" op "" oI" ~ ~:." "G4 .................... NUE] || | (raion o - .................... $00 (Ass ntsc t |- ~*~ "op ~ |/" _ dl ...... 1. YC phe- blir : 7.1 .................... 100 1 ~*~" esa n ~*~: ""~ "" op" / |:: V/ 'we .................... $00 ' |:1--*~=-~**rop~:~~|~-**'somut Asiqny 800 op- / f op "at ...... 900 ° opy ~~~ 0p ~~~" OT s 0 00 ( Dogan ls spake dI .................... 800 ' | s8uptte) osouesuepy |-oupur uspyoureddy |~~~~~~~~y1-4 'Ajunopy moj1eq : 813.1008) 0 [ETT WMI. *" Ios a o aige l mature L-EUS-CI ...... go _ |~==~=~~| 10° |~~~zaz0 |jequs Aeyr ogffe0g0g |~~~~~~~~~0-THS-CI 's} py cougp -p A014 '£jun0p outpisuIiog Uutg .................... tub | :=: "rsf mopar" ""~ "fop TTI. 000" Cu .................... 200 ° pop | ~f Op" .................... too' |: "** opt fof" ~~~ "op HT C ASF .................... 200: |""*~*~ -me r ~ Op aap Coone .................... 200 ' 'ssuts; prop | our PIO |~~~~~~~~~I-HMO-€f OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 56 ...... L 9210 ° fr %o 10° t u" 900 ° .. . LOfe sur 1 o - aplina man nato, 'oreqs ...... 800 ° STIO ® Antoaneta . 6" 10° (7 ro ao op tts soon. 1a] "~I gan ) 'oreys Jo 1oqtaour ...... 900 * 8600 * M t S00. 10 1 [Atl apy os" 400" [770 C 200° | OUOJSDUES ...... 800° | ©8600" | 500 800 | soo" soot gag : ue, |~~oreqs |~~~~~~~~"g-dL-911 'Ayunop *sSuf[te) out 20° £0 ° ©00°. |"" "22" 10} [*** : (s Uh repairs lu M till (aP pained pens go' 1"*~**~ €0° | -peor-osous@uspy |~~~~~~~~~~~~ up~" ~~~" "A"" ~ 6 *(@pe13-Aof) 9151}090U00 20 ° £0 ° €00°' "175°" £0 ' |;"~~~> 100 (7. "III"" 20" 4] ©00 ° 4 :*" etter nash rapt sou 20° osousBuepy |~~~~~~~~~*~~- Opina " 8 s8ut 10° 90 ° ..) $0 % i 11 Ui buiigaies 80" (500 [~ ~ " "fnr rf so [ou n(n" s 10° osous8uepy |~~~~~~~~~~~~ gp TI 4 10° 90 £00) : 50. F000] ""~." $0. | 800 (5. |e pca 100 ® PAT t o 200 ° esoussuep; |~~~~~~~ Rereek opr of"" 9 70 ° 10° £002 C l er omar nnn" 10" 1 $004 "sta sa ott ns clue mt copy 10 [fare l \o B fel) 10° £0 ° 00> |:." 10 Teper II*" $0 % | $00 517-5 -[" Comoro f fera -. Jie rabtidnne rote 80 ° prog ba *so7€.1}U00000 £0 * 10° £00 ° $00 : 1%" ara aon j | $00" | "~~~ 100" 179""" 400 'Of $00" [~~ OCCT 10° ©q8H0qI80 pear $ 90 ° 20 ° £00; cs if shaman U 100 'O) 100 ® |~~~~~~ $00" | 800° |-* IC "A" 901 "*-* sSupye; oupz |~~~~~ ouput |~~~~~~~~~ S-WA-91 :oaop ssedumg '&Kjunop 90 ° 90 ° ©4005 11. "~ "onan referer nsa anns €0 ' 10 (far sa" $00 eo C" 20° p1O# 'speop; |~===~~~~~~~~~ op" f "!~ € *poztptxoun F0 ° 90 ° 800 :> [I" 90 ° 1091 SIE "C" 800" £0 ° 10° ©40 pos 'speop; |~=~=~~~~~~~~~ op n"" "" 6 'oupur 90 ° 90 ° culbcs donk phage cones bree anal ©0110" (1% "p pr ~ $00 [7~"~~~ 10 1a C0. |.. ""~" POD pIég |~~~~~ TI-W§-01 'J0L9stp usfouy, 80° E ol Lapras comune aar comet Wessel 20° od onal abbey prone robe spa tT T0 ' |*~~o10 pros wwvaom ............. Op Snl oreos (d pus Suf}ssot L 80 ° $00 > 11 e aarp" 10° | 10" [." ly f ant iind eran 20° | sSurtte} prop pusprepy |~==~-~~~~~*~ T-W-OL '10L0STP soo | so' 800 :> r -= 80 1. to" 10 (2a nen ran sonst" 0° [**~**~ sSultte} plop 1ou,1 |~~~~=~~~-~ '10LI}stp '&junop 'moxeq y1n0g ...... $00 $0" (y yp arre Nairn t (Iona [arena 800 ° shield I. |) UG" .. apne s - ...... 600 ~ 1 C1 -S" IOI B0 " . (17 n pron freno feat tha o rt gob t (R= offer- onf nen [ase==«l<---- ~:~ 100 ae e rs CTRS C. sn Ara cv es laz an ". trl Is Ix 1021 ~' up~: 7 'Op 7 T 6 'so1817000 *ouput £0 ° 200 £00 yu i=. 7. [atl uae aan gol sou" ""~: |r: " 20 ° -uoo osoussuepy | UfeJunopy opeIE |~~~~~~~ I-oWD-. srupSiA '&junop y&wg £: 0 £09 > | a sC" eo sn {it" 33 Pale ipr: (ramet e (Ars 13" o 100 ' supa Pam. 9002 [42 3 o e ign ae op n | " *Aeto *(31f) sope9u00 tol} 9181190 + 1: sho '> | ax" spy Area eel aCe @r t s t {c ol £00 * F o nes" mot ool 200 »uoo osoussuept -u0o |~~~~~~~~~~ 1-IG-41 f 000 ouput 80 ° 80 ° $00 >: met spf fst fi »| Ago h "2C $* aot ( acr | oa a ¥00 * eM Al eC B 10° -uoo osoussuepy | ufe;unopy punog |~~~~~~~~~ ¢-WH-81 ot9stp wergosted -dy '4junop pusg x f *ouos - oreqs 'urequnopt ...... g got a (rors emel abo |--: 4 "" Aaa" $00 1 n (as oon gag» | agaogs ouo;spusg | ofdurop, |~~~~~~~~, :Ajunop Asourg 'TelN "snp ong 'ouput 6° 20 ' goo > (::= aar sira Cae o 100" l: zo * | soo 'of: >* "1st | erate alr a n o Re ak e 200 ° snp 10199[[00) sping |*=~~~~"°~/C 1-48-6 % sensu, 'Aqunop 10}SMOI¢ SS@L is *Apuss ...... gp: (o ee stea r gph | cha ner fsr niste gon 160.1 P 2 (P ___ "tooo "Sex"" ""~ "a"." 's 'uogs® Op ~" 8T ...... 90° |. 210° Aan {ec anes eel | o | agt nor] rer ol 006° olen s= =| «=-- 1~-~**- umosd fore "O0 S (L" ~~ 9 m % f qred | Tomo tmoq F ...... 90° |O. O10" pe | ol roel 60°. aq {seafront te t aT sd *. 400% 'quo;spweg [IO |~~~~~~~~>8-0018-#°1 W :Ayunog uosyo®f KA 'oreqs ...... 10° | 9050 ° |f "collets . Bod: (=-- s= nnn Ss [ .*.. mm + | nn af ...... Lk s00 > (: "241 "45 >, metal"": (5 tal seo" $o L {onn oren rect "o" 1900] S:" «l ropey "nano" "~*~" Seated 58 GENESIS OF BERYLLIUM DEPOSITS The physicochemical conditions under which the beryllium-bearing minerals originate have not been de- termined, with few exceptions. However, some idea of the conditions may be surmised from the relative abundance of these minerals in certain geologic envi- ronments and their virtual absence in others. The pre- ceding discussions emphasize that with few exceptions beryllium minerals occur in silicie and alkalic igneous rocks, especially pegmatites, in pyrometasomatic de- posits, and in high- to medium-temperature veins. Beryllium deposits thus are mainly the products of igneous activity, rather than of sedimentary and meta- morphic processes. Figure 3 shows the distribution PYROMETASOMAT IC DEPOSITS IGNEOUS Rocks PEGMATITES HYDROTHERMAL VEINS - -- __ ___.. _ __ __ _ Ma.. CHRYSOBERYL rELOSPAR,| mca, Etc BEXt A} PHENAKITE HELVITE ‘ _ 2 2 e - p- _o __ cl 1DOCRASE ho dtm. FreurE 3.-Schematic diagram showing occurrence and distribution of principal beryllium-bearing minerals. of the common beryllium-bearing minerals among the various types of major occurrence. Such a diagram cannot, of course, be quantitative with regard to the amount of any mineral; thus, the arrangement of col- umns is not necessarily significant. Theoretical considerations discussed by Osborn (1950) lead to the conclusion that beryllium should be concentrated in the late aqueo-igneous residue of a magma, as a result of fractional crystallization, along with Si, F, Li, Na, K, and rare earths. These elements, together with water, generally are not removed in pro- portion to their abundance in the magma during the crystallization of olivine, pyroxene, amphibole, and plagioclase, which constitute the bulk of earlier min- erals in igneous rocks. Their proportions in the re- maining liquid, therefore, tend to increase progressively with crystallization, which is controlled largely by the concentration and stereochemical properties of the ions. Temperature is regarded as more important than pressure. Distribution of beryllium in igneous rocks and min- eral deposits suggests that much of it is deposited in beryl and helvite during the transition from magmatic OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES to hydrothermal conditions. Except for local occur- rences in granite, beryllium minerals are rare in igneous rocks other than pegmatites; probably most of the beryllium in such rocks is contained in silicate structures as a guest ion. This tendency appears to be particu- larly marked in the feldspathoidal intrusive rocks, which do not as a rule give rise to extensive pegmatites and ore deposits. Most veins containing beryllium min- erals are of high-temperature origin and may form about the same time as pegmatites and pyrometasomatic deposits. The reasons for deposition of beryllium in peema- tites or veins at some localities and in pyrometasomatic deposits at others are not clear, In the Victorio Moun- tains, N. Mex., beryl crystallized in an open vein about the same time that helvite replaced limestone nearby. Most pyrometasomatic deposits do not have any direct relation to pegmatites or even to neighboring igneous rocks. In pyrometasomatism the ease and pervasive- ness of replacement implies high concentration of water and other volatiles. Although a moderate concentra- tion of volatiles appears necessary for the growth of large crystals in pegmatites, detailed studies of their structure and composition suggest that they are formed from an equivalent body of magmatic material, with only minor and later hydrothermal alteration (Cam- eron and others, 1949, p. 97-106). According to this view, preexisting fissures are required for emplacement of pegmatites, whereas pyrometasomatism may be ac- complished through rock pores without recourse to larger openings. Veins are regarded usually as fissure fillings. In a general way, structural conditions may thus influence to some extent the modal occurrence of beryllium in that commonly beryl appears to prefer fissure deposits and helvite to favor replacement bodies. Structural features presumably have little to do, how- ever, with the presence or absence of beryllium in the deposits. Whether beryllium appears at a given locality pri- marily in pegmatites, in veins, or in pyrometasomatic deposits is concerned also with relations of the pegma- tite melt and the hydrothermal fluid. Petrologists do not agree on whether the two fluids exist as separate phases in the rest magma or are parts of a single water- silicate system. Objections by Morey (1949) to the hypothesis of immiscible fluids as postulated from theo- retical studies by Neumann (1948) and the qualitative experiments of Smith (1948), seem to have been re- moved by recent quantitative experiments proving im- miscibility in systems similar to magmas (Tuttle and Friedman, 1948). It remains to be proved that such immiscibility did in fact exist in the natural processes of pegmatite and vein formation. COMMERCIAL POSSIBILITIES AND In practice, the distinction between quartz-rich peg- matites and quartz veins is actually somewhat arbitrary ; in this investigation those bodies with an appreciable amount of feldspar were considered as pegmatites. Many examples of gradation between the two have been described (see compilations by Tolman, 1931, and Fur- nival, 1939) and the beryl-bearing veins of Mount An- tero, Colo., Hill City, S. Dak., Irish Creek, Va., and several foreign localities are all described as being closely related to neighboring pegmatites. Fersman (1940, p. 37-39) emphasized the genetic relation of many quartz veins to pegmatites, and recent structural studies of pegmatites have shown that many quartz-rich (and sometimes beryl-bearing) fracture fillings are continu- ous and contemporaneous with the quartz core or other inner zone of the associated pegmatite (Cameron and others, 1949, p. 70-83, 105-106). These associations suggest that some beryl-bearing quartz veins have an origin similar to pegmatites, if they are not actually continuations of neighboring pegmatites. They were probably formed at high temperatures from "magma- like liquid" (Jahns, 1948). The temperatures of formation of pegmatites, pyro- metasomatic deposits, and hypothermal veins probably are similar. The prevalence of helvite and idocrase in pyrometasomatic deposits in contrast to beryl in peg- matites and veins is, therefore, probably due to chemical environment rather than to temperature. In syenitic pegmatites, helvite or rare aluminum-poor beryllium minerals occur, whereas, in pyrometasomatic deposits in aluminous schists the mineral is beryl. Such occur- rences are rare, however, as most pegmatites are gran- itie and most pyrometasomatism is in calcareous rocks. Where the ratio of aluminum to calcium, sodium, and potassium, is greater than one, some aluminum is avail- able to form beryl; otherwise helvite may form (Holser, 1953, p. 608). A somewhat wider range in temperature of formation is noted for helvite than for beryl. In pyrometasomatic deposits helvite is generally late in the mineral sequence, often lining vyugs. The manganese-rich veins in which it occurs apparently formed at a lower temperature than the beryl-bearing quartz-tungsten veins. The as- sociation of a nearly pure manganoan member of the helvite series with sphalerite in veinlike deposits in the Carpenter district, New Mexico, in contrast to the oc- '\ currence of zinc-rich genthelvite in the pegmatites at St. Peters Dome, Colo. (Genth, 1892), suggests that at least this helvite-bearing vein was formed at a tem- perature far enough below that of pegmatites to de- crease considerably the solubility of zinc in the helvite lattice. The thesis that beryllium tends to be concentrated SUGGESTIONS FOR PROSPECTING 59 in the late silicic and alkalic differentiates of igneous magmas is based on averages of many analyses rather than on specific examples. In some igneous rock series whose trace elements have been analyzed in detail (Nockolds and Mitchell, 1948; Wager and Mitchell, 1943), the amount of beryllium concentrated in the final differentiates (granophyre and aplite) is too small to be detected by qualitative spectrography. Although analytical data indicate that granitic and syenitic rocks are on the average richer in beryllium than mafic rocks, some granodiorites and other intermediate types con- tain appreciable quantities of beryllium. These dis crepancies may be due, of course, to differences in beryllium content of the magmas involved, but it is not certain that beryllium is inevitably concentrated in the late magmatic products. At Mount Antero, Colo., and Bagdad, Ariz., rather complete gradation is found from a granite so rich in beryllium that it occurs as grains of beryl, through beryl bearing schlieren, vugs, and small veins to conventional pegmatites. Such deposits have not been sufficiently studied to determine the relations between beryl and other rock minerals. However, in the Sheeprock Moun- tains, Utah, beryl replaces feldspar in an albite granite and appears to have been introduced in connection with albitization of the granite. ( The concentration of beryllium in pegmatites may have been exaggerated. Moderately rich beryl pegma- tite ore contains only about 1 percent beryl, or about 0.1 percent BeO (Hanley and others, 1950, p. 11). This does not take into account beryl that is too fine grained for hand sorting or that lies in unmined zones. If one considers that only a small percentage of pegmatites contain enough beryl to be mineable, it is apparent that the overall average beryllium content of pegmatites may not be appreciably higher than that of the average granitic or feldspathoidal rock. Many sedimentary rocks and residual deposits con- tain some beryllium and beryllium shows some tendency to follow aluminum in sedimentary processes. -For the most part, however, beryllium probably tends more to be dissipated than concentrated by processes of weather- ing and sedimentation. Little information is available concerning the beryllium content of metamorphic rocks, but there is no indication that beryllium tends to be concentrated by processes of dynamic and regional meta- morphism. j COMMERCIAL POSSIBILITIES AND SUGGESTIONS FOR PROSPECTING The deposits of beryllium in nonpegmatite rocks that are most likely to be of commercial interest fall into two categories: beryl in high-temperature veins and % 60 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES igneous rocks, and helvite in pyrometasomatic deposits. Beryllian idocrase commonly occurs with helvite, though it is probably never high enough in beryllium content to make its separation profitable. Its effect, therefore, is to make some of the beryllium contained in the deposit economically unrecoverable. Other sili- cates which contain beryllium, such as garnet and epi- dote in pyrometasomatic deposits, and micas and feld- spars in igneous rocks, have a similar but lesser effect. The best nonpegmatite beryllium deposit yet discoy- ered is that at Iron Mountain, N. Mex., where a small tonnage of high-grade tactite ranges from 0.5 to 3.5 percent BeOQ, with an average of less than 1.0 percent, mostly in helvite. 'The low-grade material ranges from 0.1 to 0.85 percent BeQ, with an average of 0.3 percent, but only a small part of this beryllium occurs in helvite (Jahns, 1944a, p. 59). Vein deposits in Arizona and New Mexico contain from 0.01 to 0.1 per- cent BeQ, presumably all in beryl. These grades com- pare very favorably with those of beryl pegmatites, where the zones mined for beryl range from 2 percent down to less than 0.1 percent beryl, or about 0.2 to 0.01 percent BeQ. Despite the fact that several thousand tons of high- grade material are indicated at Iron Mountain, the deposit has not been mined, principally because it is fine grained. In inner pegmatite zones, some of the beryl erystals which are several feet long are easily hand sorted, or selectively mined, to give a concentrate above the marketable minimum of 8 percent BeQO. Such treatment is impossible with the fine-grained ma- terial of all nonpegmatite beryllium deposits. Flota- tion of both beryl and helvite ores has been moderately successful on a laboratory scale (Lamb, 1947; Sned- don and Gibbs, 1947; Kennedy and O'Meara, 1948). However, when metallurgical concentration becomes widely applied to fine-grained beryl, the nonpegmatite deposits that could be worked would still have to com- pete with pegmatite deposits, many of which also con- tain beryl too fine grained for recovery by sorting. In the Black Hills pegmatites, no deposits have been mined exclusively for beryl, it having been recovered as a byproduct of mica, feldspar, or lithium-mineral mining (Page and others, 1953, p. 52). | Similarly, byproduct recovery of fluorite and magnetite may make it possible to mine the Iron Mountain tactite at a profit. Prospecting for nonpegmatite beryllium should be only part of a general prospecting program, as the beryllium can probably be recovered only in conjunc- tion with some other metal or mineral. Actually the greatest hope is probably in byproduct recovery of beryllium from high-temperature veins or pyrometa- somatic deposits that are presently producing a large tonnage of ore for tungsten, gold, lead, or other metals. The possibility is indicated by recovery at Climax, Colo., of cassiterite from molybdenum ore containing only a trace of tin (Gustavson and Umhau, 1951, p. 1195). , Where a large proportion of the beryllium is dissem- inated in minor amounts through the principal rock minerals, instead of occurring as beryl or helvite, the problems are much greater. High temperatures or very strong acids are required to decompose silicates such as idocrase, nepheline, and garnet and release their beryllium. Recovery of beryllium from such minerals does not seem likely at present. Even for minerals more susceptible to chemical treatment, such as the cryptomelane of Golconda, Nev., recovery would be relatively expensive. Traces of beryllium in minerals might be recovered as a byproduct in smelting to re- lease other metals. However, most smelters treat mainly sulfide ores, which are unlikely to contain beryl- lium. Sampling of many zinc, lead, and copper smelt- ers by the Mine, Mill, and Smelter Survey showed no beryllium in any of the products. Nonsulfide ores, such as bauxite, have a remote possibility of producing beryl- lium, but bauxites from the United States apparently contain very little. The lack of a reliable method of beryllium analysis, with the attendant problem of separating ore from waste during mining, is an important economic factor. Although some pegmatite beryl is difficult to recognize, the problem is greatly increased when the material is fine grained. At Iron Mountain, N. Mex., much of the helvite-danalite cannot be distinguished from garnet except by a stain test. Some or all of the beryllium in- dicated by chemical or spectographic analyses may be contained in rock minerals as a guest element rather than in beryllium minerals. Microscopic mineralogical analysis is therefore recommended as offering the most realistic estimate of recoverable beryllium. Occasional control determinations of total beryllium content might be made by spectrography. The importance of nonpegmatite beryllium deposits is exemplified in the Soviet Union. According to Scherbakov (1936) the Izumrudnie (emerald) mines of the Southern Urals have greater possibilities than all the other regions of the Soviet Union as a source of beryllium. Although associated with berylliferous peg- matites, the principal deposits are in the surrounding schists and slates. The second most important are the Sherlovoi Mountain deposits in Zabaikal, where beryl occurs in quartz veins and greisen zones in granite. Al- though none of the deposits thus far discovered in the United States is exactly analogous to these, the possi- bilities for discovery are not exhausted. LOCALITIES IN NEVADA AND CALIFORNIA 61 Most prospecting for nonpegmatite beryllium prob- ably will be confined to pyrometasomatic deposits and high-temperature veins. The relationship of beryllium and fluorine minerals has been noted in many of these deposits, and the association of idocrase and fluorite in pyrometasomatic deposits is thought to be a reliable guide to beryllium occurrence. between beryllium and tungsten is suggested by the widespread occurrence of beryllium in tungsten-bearing tactites and veins. In general, mineralogical criteria appear to be some- what more reliable than structural features, though the latter may also be clues to beryllium occurrence. Some beryllium-bearing tactites show a peculiar banded structure, called "ribbon rock" at Iron Mountain, N. Mex. Material of this type was not found during the present investigation in any of the beryllium-bearing tactites. Similar banded magnetites were completely free of beryllium. The absence of this structure, there- fore, does not preclude the possibility of the occurrence of beryllium in tactites ; that all "ribbon rock" contains beryllium remains to be proved. Most pyrometaso- matic deposits that contain beryllium are found near the contact of limestone and granodiorite or granite. However, beryllium-bearing tactites, like other pyro- metasomatic deposits, commonly being controlled by fractures or high-porosity limestone, may not be closely related to contacts. At Iron Mountain and Victorio Mountains, N. Mex., intrusive rocks are relatively in- conspicuous. As beryllium comes into greater use and the present resources are exhausted, it will become increasingly necessary to find new resources by scientific means. For this purpose a really basic understanding of the geo- chemistry of beryllium is necessary, especially an un- derstanding of the relations among beryllium-bearing minerals, and the physical and chemical conditions of their deposition. Further investigations of the natural occurrences should be supplemented by experiments un- der controlled laboratory conditions. DESCRIPTION OF LOCALITIES NEVADA AND CALIFORNIA By E. N. Canprox and L. A. Warner Sampling of nonpegmatite rocks and mineral de- posits in Nevada and central California was undertaken by Cameron, assisted by J. H. McLeod, during July and August 1949. In the short time available only a few of the many mining districts of the region could be ex- amined. Locations of the 27 districts and areas selected for investigation are shown on figure 4. One of these, the Tem Piute district, had been sampled by the Geo- A similar relation | logical Survey in 1943 and was not revisited. Cameron found it necessary to return to other work before com- pletion of the laboratory investigations. The analytical data were compiled by Warner, who also wrote parts of the descriptions. The descriptions of deposits are based partly on observations made during the sampling, but free use was made of information in the literature and of unpublished reports and maps compiled by var- ious geologists of the U. S. Geological Survey during World War II. Of the more than 300 samples that were collected and analyzed spectrographically for BeO, the larger num- ber are from tungsten deposits in which scheelite is the dominant tungsten mineral. The field itinerary, therefore, conforms in a general way to the tungsten ares in the Basin and Range province as shown by Kerr (1946a, pl. 1). A variety of other materials, how- ever, was sampled in Nevada, including the manganese and tungsten-bearing hot-spring deposits at Golconda and Sodaville, the barite deposits at Good Hope and near Battle Mountain, andalusite deposits near Thorne, brucite-magnesite deposits at Gabbs, and a dumortierite deposit near Oreana. Samples of igneous rocks and contact-metamorphosed sedimentary rocks in and ad- jacent to the ore deposits were obtained in nearly all districts visited in which contact metamorphic tungs- ten deposits occur. The analytical results suggest that in this region beryllium occurs in greater concentrations in the tungs- ten-bearing tactite than in the other deposits sampled. Of the 4 samples containing more than 0.01 percent BeQO, 3 were from tactite deposits at the Star, Victory, and Rose Creek mines; they contained 0.056 percent, 0.044 percent, and 0.024 percent of BeQ, respectively. Samples containing more than 0.001 percent BeQ were obtained from all tactite deposits, though the average for some deposits-particularly at the Desert, Gun- metal, and Ragged Top mines and deposits in the Raw- hide district-is considerably less than this amount. The BeQ content of samples from tactite in the Mill City district, Nevada, and the Tungsten Hills district, California, were relatively low in comparison to the importance of these districts as tungsten producers. In general there is no apparent correlation between the amounts of tungsten and beryllium in the tactite deposits. The beryllium content of the tungsten-bearing tactite is in marked contrast to that of associated horn- fels, marble, and quartzite. Though many samples of these rocks were obtained, none contained BeQ in excess of 0.001 percent. The beryllium contents of igneous rocks associated with the tactite is also low, the few exceptions being for samples obtained adjacent to con- 62 OCCURRENCE OF NONPEGMATITE 120° 42 BERYLLIUM IN THE UNITED STATES 114° EXPLANATION PSH Locality sampled for this report X5 Other sampling Des fee ie fans' District having sample containing 15 Elko more than 0.005 percent beryllia p Wells NEVADA Elko County 1. Star mine, Harrison Pass 2. Good Hope mine Humboldt County 3. Golconda deposit 40° Lander County 4. Battle Mountain barite deposits Lincoln County 5. Tem Piute district Mineral County Rawhide district Desert Scheelite and Gunmetal mines Sodaville district Thorne andalusite deposits Nye County 10. Victory Tungsten deposits 11. Gabbs magnesite and brucite 6. T. 8. 9. Pershing County 12. Limerick Canyon area 13. Panther Canyon area 38 14. Rocky Canyon-Wrights Canyon area Tungsten area 16. Rose Creek mine 17. Ragged Top mine 18. Champion dumortierite mine White Pine County 19. Cherry Creek district 20. Sacramento Pass mine 21. Dirty Shirt mine 22. San Pedro mine 23. Minerva district <> anne ao wee h ae comme n me me me CALIFORNIA Inyo County 24. Tungsten Hills district 20. Pine Creek district 26. Yaney prospect % meen ax os mcse a ie ©27 Bakersfield o . San Bernardino and Kern Counties 27. Atolia district 36° 118° 40 0 Cran sct 4 1 1 116° 120 Miles FIGURE 4.-Index map showing localities sampled in Nevada and California. tacts with tactite, where endomorphism might be ex- pected. These relations imply that beryllium was in- troduced by ore-forming solutions which gave rise to the tungsten-bearing tactites, the two metals being de- rived from a common magmatic source. Several scheelite vein deposits were sampled in the Snake Range and Cherry Creek district, Nevada, and in the Atolia district, California. None of the samples con- tained more than 0.001 percent BeO and most contained less than 0.0001 percent. The paucity of beryllium in these veins, in contrast to its relative abundance in pyrometasomatic deposits nearby, apparently is more marked in the Basin and Range province than in other areas where beryl is not uncommon in quartz-tungsten veins. The beryllium-bearing hot-spring deposits of Pleistocene age at Golconda and Sodaville, Nev., must be regarded as extraordinary. These are ocherous de- posits containing relatively large amounts of manga- LOCALITIES IN NEVADA 63 nese and tungsten. A sample from the deposit at Gol- conda contained 0.016 percent BeQ, and one from Soda- ville contained 0.0075 percent. NEVADA ELKO COUNTY STAR MINE, HARRISON PASS The deposits of the Star mine are in the Ruby Range on both sides of Harrison Pass Creek Canyon, about 2 miles east of the pass. They are readily accessible by road from Elko by way of Jiggs, thence by the road over Harrison Pass. The area is described briefly by Hess and Larsen (1921, p. 305) ; the deposits were mapped by M. R. Klepper and P. Joralemon of the U. S. Geological Survey in 1948. The Ruby Range consists largely of a stock of biotite granite and quartz monzonite that intrudes limestone and quartzite of Paleozoic age. The contact east of Harrison Pass is very irregular; and many dikes and apophyses of aplitic granite cut the sediments, which have been metamorphosed to silicated marble and horn- fels. Scheelite-bearing tactite occurs intermittently along the contact. Four ore bodies have been mined on the property of the Star mine and several others have been prospected. The principal workings, which are in the Main, North, and South ore lodes, were inaccessible in 1949. The No. 7 ore body and the ore bodies in the North opencut and the South shaft were examined briefly. The North opencut exposes a tactite body along the irregular boundary between granite and marble. The body is 1 inch to 30 inches thick, not more than 20 feet long, and probably contains no more than 200 tons of rock. The tactite consists of garnet, diopside, epidote, quartz, and calcite. The South shaft ore body is a tactite mass about 200 feet in strike length and 1 to 4 feet wide. A vertical shaft, 43 feet deep, has been sunk near the middle of the outcrop. From the bottom of the shaft a drift ex- tends along the base of two stopes; the south stope is blind, the north stope extends to the surface. The tactite body appears to be cut off at depth either by a fault or by a change in strike of the contact of the granite and marble. Reserves are no more than a few hundred tons. A belt about 1,500 feet wide along the irregular cast- ern margin of the granite stock consists of marble, sili- cate-bearing marble, and cale-silicate hornfels. 'The beds range from fractions of an inch to 3 feet in thick- ness. Garnet, diopside, and epidote are the principal minerals, but actinolite, idocrase, and tremolite char- acterize some beds. Samples were taken of the metamorphosed rocks of the contact aureole, as well as of the tactite deposits. - Sample descriptions and analytical results are given in the table 17. Tasun 17.-Beryllia in samples from Harrison Pass area BeO Sample Description (percent) NORTH OPEN CUT 329-1039 Chip sample of aplitic granite 10 to 30 ft from 0. 0002 1040 Chip sample of tactite_._._.---------.-- . 0044 1041 Chip sample altered aplitic granite im- mediately adjacent to . 0098 1042 Silicated marble 0 to 3 ft from tactite.__- <. 0001 soUTH SHAFT ORE BODY 329-1043 Chip sample of tactite body, north end of south stope at its base._______------- . 029 1044 Chip sample from tactite body, top of south stope. . 056 1045 Chip sample of silicated marble adjacent to tactite, bottom of north stope.-__. .. <. 0001 1046 Chip sample of silicated marble adjacent to tactite, base of shaft__________---- <. 0001 1047 Chip sample of granite outcrop adjacent to tactite, north of shaft____.___------ . 0078 CONTACT-METAMORPHOSED ROCKS 329-1048 - Chip sample of recrystallized marble, 0 to 15 It from.contactl .-.. <. 0001 1049 Chip sample of blue and gray marble, partly silicified, 15 to 70 ft from con- Tach... <. 0001 1031 Chip sample of blue and gray silicified limestone, 150 to 170 ft from contact.. <. 0001 329-1054 Chip sample across beds of idocrase- bearing(?) marble, 345 to 365 ft along s road from contact l...........l...... <. 0001 1055 Chip sample of interbedded pure and sili- cated marble, 656 to 681 ft from con- TACY:L :. . _ ...d. c aan - us. <. 0001 1057 Chip sample across beds of bluish-gray, fine- to medium-grained marble, 1,053 to 1,233 ft along road from contact.... . 0008 1059 Chip sample across beds of blue-black limestone, 1,520 to 1,540 ft along road from Contact.} Jel . 0008 1061 - Chip sample of silicated marble and horn- fels, south slope of Harrison Pass Creek Canyon, between No. 7 ore body and Main ore body... <. 0001 1063 Chip sample of porphyritic granite, sum- mit of Harrison <. 0001 The analytical data clearly indicate that beryllium is contained in the tactite bodies and in the granite imme- diately adjacent to them. It appears to be lacking in the other rocks of the contact aureole and in the interior of the granite stock. Presumably the solutions that formed the tactite bodies and related tungsten ores were those which brought in beryllium. The beryllium-bear- ing mineral or minerals have not been identified. If most of the beryllium is in helvite, some byproduct re- covery may be possible in connection with future min- ing of tungsten in the area. GOOD HOPE BARITE MINE, TUSCARORA RANGE The Good Hope mine is on one of a series of barite vein deposits in the Tuscarora Range. The mine is 64 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES reached by a road leading north to Lynn from U. S. Highway 40 at Carlin, Nev. At 74 miles from U. S. 40 and just south of the mouth of Maggie Creek Can- yon, a mine road turns westward. The mine is about 1.3 miles from this point on the northeast side of a small canyon. The deposit, as exposed in the main and upper work- ing, is an irregular vein of massive, fine- to coarse- grained, white barite that apparently occupies a shat- tered zone in partly silicified interbedded limestone, shale, and sandstone. The vein strikes N. 38° W. and dips 70° to 80° E. The lower working consists of a 41-foot drift along the vein, which is 4 to 5 feet wide, and an adit that extends northward from the mouth of the drift. A chip sample (329-1071) of the vein from the upper working contain 0.0007 percent BeQ. HUMBOLDT COUNTY GOLCONDA MANGANESE-TUNGSTEN DEPOSIT The Golconda manganese-tungsten deposit is in the Edna Mountains about 3 miles east of Golconda. The mine is a short distance north of U. S. Highway 40 and immediately east of the road to the Getchell mine. The deposit has been described by Kerr (1940; 19462, p. 171-178). It was mined for manganese during World War I and for tungsten during World War II. The deposit consists of layers of manganiferous ocher and calcareous tufa, with some rubble derived from un- derlying Triassic sedimentary rocks, and is capped by tufa and fanglomerate. The ore bodies extend north- ward along the slopes for about a mile. Toward the east they rest directly on the beveled edges of the Trias- sic sedimentary rocks, but toward the west an increas- ing thickness of sedimentary rocks intervenes between the deposits and the bedrock surface. A typical pedi- ment-alluvial fan relation is indicated. The tungsten- bearing manganese oxides and ferruginous ocher, to- gether with the tufa, were deposited by hot springs thought to have been most active during the Pleistocene epoch. Fissure veins in the underlying Triassic sedi- mentary rocks contain ore material similar to that in the overlying ocherous deposits. For the present purpose the workings are divided into two groups: the north workings, which consist largely of opencuts and stopes, and the south workings, which are a series of large opencuts. U NORTH WORKINGS The workings of this group may be subdivided into the northwest workings, which are a series of adits that lead to gently inclined stopes, and the Bed Springs Hill workings, which consist of opencuts around the eastern end of the hill and underground workings of unknown extent. In the northwest workings, two parts of the stopes were sampled. The section exposed in the stopes is as follows, from top to bottom : 4. Thin layer of gravels. 83. Coarse rubble (fanglomerate?) cemented by calcareous tufa ; as thick as 6 feet. This is the cap of the deposit. 2. Rubble tufa with manganese oxides and ocher, 1 to 3 feet thick. Apparently this zone was mined for manganese. 1. Rubble poorly cemented by tufa. Thickness more than 3 feet; bottom is not exposed. Contains some manganese oxides and ocher, but much less than zone 2. At Bed Springs Hill, in the opencuts near the north end, the beds dip gently westward and are as follows, from top to bottom : 5. Thin layer of gravels. 4. Calcareous tufa caprock, as thick as 5 feet. inches in places is manganese rich. , 3. Layer rich in manganese oxide and ocher, ranging along strike from iron-rich to manganese-rich; 9 to 18 inches thick. 2. Gray shale rubble as much as 2 feet thick. Low in man- ganese and iron content. 1. Soft shale of Triassic age, forming the surface upon which zones 2 to 5 were laid down. Manganiferous and fer- ruginous. This material has been mined to a depth of at least 10 feet in the opencut. The lower 12 Descriptions and analytical data for samples from the north workings are given in table 18. TaBur 18. -Beryllia in samples from north workings, Golconda - manganese-tungsten deposit BeO Sample Description (percent) BED SPRINGS HILL 329-1073 Chip sample, calcareous tufa, zone 4. ___ 0. 0008 1074 Chip sample, manganese-rich material, base of zone A...li clu el. . 0026 1075 Channel sample, manganese-rich material, € LONG 3...2. cage onun sn sewa a ess . 0045 1076 Channel sample, ocher-rich material, one ~ . 0037 1077 Channel sample, zone . 0016 1078 Chip sample, small lens of ocherous tufa in wone' tios _L... ion:" _2 lz f r ROO" . 0058 NORTHWEST WORKINGS 529-1079. Chip sample, zone . 0007 1080 - Channel sample, zone . 0058 1081 - Channel sample, zone . O01 SOUTH WORKINGS The south workings consist of three large opencuts arranged roughly along a line trending northeast for about 2,000 feet. The northeastern cut is about 600 feet long and 200 feet in maximum width; the middle one measures about 700 feet by 700 feet. The southeastern cut was not measured. It is the largest and deepest of the three cuts, but its walls are not accessible for sampling. LOCALITIES IN NEVADA In the northeastern cut the section is as follows, from the top down : 4. Tufa cap, more than 3 feet thick. 3. Manganese-rich layer, thickness greater than 4 feet; bottom not exposed. Mined in underground workings of unknown extent. 2. Shale rubble, at least 4 feet in maximum thickness. This material is highly variable. In part it appears nearly barren of iron and manganese oxides, in part it is rich in one or the other. 1. Shales of Triassic age containing manganese and iron oxides. In the middle cut samples were obtained from the east wall and the southwest wall. Along the east wall the section is as follows, from the top downward : 4. Fanglomerate, 6 to 8 feet thick; rests on the uneven top of of a layer of compact calcereous tufa. 8. Calcareous tufa, 3 to 7 feet thick, bottom gently undulating. 2. Manganifereous fanglomerate, 9 inches to 2% feet thick. 1. Ferruginous fanglomerate, thickness more than 4 feet; bot- tom concealed. ' Along the southwest wall the section is as follows: . Fanglomerate, a maximum of 4 feet in thickness. . Manganese-bearing, fractured tufa, 3 to 4 feet thick. . Manganese-rich tufa, 2 to 3 feet thick, forming a series of lenses in the tufa cap. The largest lens is about 30 feet long. 2. Manganese-free tufa, 4 to 414 feet thick. 1. Crossbedded green and brown gravels, containing ocherous layers and manganiferous layers as thick as 2 inches. Q9 a Ot Data for samples from the south workings are given in table 19. TaBur 19.-Beryllia in samples from south workings, Golconda manganese-tungsten deposit BeO Sample Description (percent) NORTHEASTERN CUT 329-1084 Channel sample, zone 8._______________ 0. 0023 1085 Channel sample, manganese-rich rubble, zone 2, southeast wall of cut_________. . 0023 1087 Chip sample, ocherous material overlying shale rubble of zone 2, southeast wall O UDE - nol 2a nra inne bee a ae an aan male . 016 1086 Composite channel sample, zone 1... . 0024 MIDDLE CUT, EAST WALL 329-1088 Chip sample, zone 3-__________________ <. 0001 1089 Composite channel sample, zone 2-..___. . 0085 1099 Composite channel sample, zone 1... . 0002 MIDDLE CUT, SOUTHWEST WALL 329-1092 Chip sample, sone . 0027 1094 Chip sample, zone 1-......._._L.. _L... . 005 OCCURRENCE AND DISTRIBUTION OF BERYLLIUM Analytical data indicate that beryllium in the Gol- conda deposit is contained mainly in the manganiferous ocher, which has been mined for its tungsten content, rather than in the tufa caprock or the underlying Triassic sediments. Presumably, the beryllium is genetically related to solutions which deposited the 467945-59--6 65 tungsten-bearing material. According to Kerr (1940, p. 1385-1387), warm spring waters rose along fissures in the Triassic rocks, the outflow resulting in beds of calcareous tufa, together with tungsten-bearing limo- nitic and manganiferous material. He concludes that iron and manganese were precipitated as gel products, which adsorbed tungstic oxide from the solutions, a process which could just as well result in the presence of beryllium. Tungsten occurs in hydrated ferric oxide, psilomelane, and hollandite; the beryllium-bearing minerals are not known. The thickness and composition of the layers in the Golconda deposits are extremely variable along strike and dip. Only detailed exploration and sampling would serve as a basis for estimating reserves. LANDER COUNTY BARITE DEPOSITS, BATTLE MOUNTAIN AREA Many barite deposits, some of commercial impor- tance, are found in northern Lander County, northern Eureka County, and west-central Elko County, espe- cially in the Tuscarora and Shoshone Ranges. The barite deposits are of two general types: vein deposits of white barite, in some areas associated with metallif- erous deposits; and bedded gray barite generally con- sidered to have formed by replacement of limestone. The veins have supplied small tonnages of barite, some of exceptional purity. The bedded deposits contain large tonnages of barite ranging from 80 to 93 percent barium sulfate and are the main producers. Samples from deposits of the latter type were obtained from mines of the California-Nevada Barite Co. and the Barium Products Corp., Ltd. CALIFORNIA-NEVADA BARITE CO. MINE The California-Nevada Barite Co. mine is reached by about 2 miles of steep but well-graded gravel road that turns south from U. S. Highway 40 at a point 12.9 miles east of the junction of U. S. Highway 40 and State Highway 8A. The mine is near the crest of the northwest spur of the Shoshone Range. The workings are a series of opencuts extending for about 2,200 feet along the eastern side of the ridge. The principal workings are in the southern 900 feet and consist of five opencuts and several minor open- ings. The workings are in a belt 300 feet wide that trends about N. 20° W. The mine is owned and oper- ated by the California-Nevada Barite Co., subsidiary of the Glidden Co. The deposit consists of beds of barite, with an ag- gregate thickness of at least 40 feet, interbedded with thin beds of chert, silicified limestone, and shale. The barite beds mostly range from an inch to a foot in 66 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES thickness and appear to be thickest and least inter- rupted by chert partings in the southern 900 feet. The structure of the deposit is highly complex. The barite beds in general appear to be dipping to the east at moderate angles, but there is local folding and much faulting. Table 20 gives the beryllia content of samples. Tasus 20.-Beryllia in samples from the California-Nevada Barite Co. mine Sample Description (pgieont) 329-1064 Chip sample, bed by bed of about 15 ft of chert beds immediately above main barite .cn... e- =- ene tad <0. 0001 1065 Chip sample, bed by bed across main barite zone; represents about 30 ft of beds.. L clon eet reas eae mall ale a a aad ors <. 0001 1066 Chip sample, bed by bed, of 5 ft of inter- bedded barite and chert immediately beneath footwall of main barite zone.. . O01 BARIUM PRODUCTS CORP., LTD., MINE The Barium Products Corp., Ltd., mine is 26 miles south of Battle Mountain in Lander County, by way of State Highway 8A. A good gravel road leads from the highway about a mile to the mine. The workings consist of an opencut about 260 feet long, 210 feet wide, and 20 feet in maximum depth. The deposit is a warped and moderately faulted , westward-dipping sheet that extends from the crest of a low hill down the northwest slope for about 280 feet. The deposit is probably about 375 feet in strike length. The barite is similar to that at the California- Nevada Barite Co.'s mine. It overlies thin-bedded chert. The overlying beds are not exposed. A bed-by-bed chip sample (329-1072) taken across a 20-foot thickness of barite, beginning a few feet above the footwall contains 0.0007 percent BeQO. LINCOLN COUNTY TEM PIUTE DISTRICT Scheelite-bearing tactite deposits occur at the north end of the Tem Piute Range in the west-central part of Lincoln County, Nev., about 85 miles west of Cal- iente. The district is reached by 40 miles of desert road from U. S. Highway 93 at Crystal, near Hiko. The principal mines of the district are the Lincoln and the Schofield, the former accounting for most of the production. A mill at Hiko processes the ore. The deposits were explored by the U. S8. Bureau of Mines in 1942 and 1944 (Binyon, Holmes, and Johnson, 1950), and were mapped and described by D. W. Lemmon (written communication). The district comprises steeply dipping limestone, shales, and sandstones of Paleozoic age which have been intruded by two small granite stocks and several nar- row basalt dikes. For a distance of 700 feet from the granite contacts the limestone is bleached and in places recrystallized. Shales are altered to hornfels and sand- stones to quartzite. West of the south stock are thick tactite bodies in bands parallel to the bedding; little tactite has been found near the north stock. Minerals observed in the tactite and listed in approx- imate order of abundance are: garnet, quartz, actino- lite, calcite, fluorite, pyrite, pyrrhotite, diopside, sphal- erite, scheelite, chlorite, hematite, clinozoisite, epidote, molybdenite, and powellite. Most of the scheelite oc- curs in garnet tactite but some rich deposits have been found in small masses of calcite-fluorite-sphalerite rock formed in marble remnants adjoining tactite bodies. Products of the mill at Hiko were sampled for the Mine, Mill and Smelter Survey in 1943. Data for these samples are given in table 21. Tasus 21.-Beryllic in mill products from the Tem Piute district Sample Description BeO (percent) 49-DGW-20 Grab sa 1gle of scheelite tailings, and sulfide float tails (1942—43 produc- MON) , 52 Lunt Je lll e we ai aan ae at 0. 002 21 Same (1940—42 production)....-........ . 003 22 Grab sample of test run on scheelite mill -.. . a Wile mme . O01 23 Scheelite concentrate (composite of samples collected by company).... . O01 MINERAL COUNTY RAWHIDE DISTRICT Tactite deposits containing scheelite occur in the southern part of the Sand Springs Range about 4 miles east of the old mining camp of Rawhide. The deposits are in sees. 1 and 12, T. 18 N., R. 32 E., near the south border of the Carson Sink quadrangle. The deposits can be reached by a graded road that turns off U. S. Highway 50 about 35 miles east of Fallon, on the east slope of the Sand Springs Range just below the sum- mit, or by graded roads leading northeasterly for about 45 miles from the town of Hawthorne. The deposits were mapped by R. F. Stopper and others of the U. S. Geological Survey in 1944. The geology of the area and locations of the mines are shown on figure 5. The Nevada Scheelite, Hooper No. 2 and Yankee Girl mines were visited and sampled. The tungsten deposits are tactite bodies in meta- morphosed limestone and hornfels at or near the mar- gins of a body of granite about a mile wide in outcrop. The limestone is part of a thick sequence of folded and faulted sediments and metavoleanic rocks that were in- truded by granite. The main limestone unit is esti- mated by Stopper (written communication) to be 400 to 750 feet thick. Other limestone units are thin beds included in hornfels that overlies the main limestone unit. The productive deposits are along the west and north margins of the granite where for some thousands LOCALITIES IN NEVADA 67 Wt EXPLANATION Alluvium 4 o Mt lin f KOS. %B Volcanic rocks l *}" MEX, gy a ars coas: ys g NM - FA e__ Granite 2 Upper metavolcanic rocks 7 gill. f6. Hornfels 8 -- s A NEVADA 'r S o MIN Contact Dashed where approximately located or inferred I: Fault Ss Dashed where approximately located ¢ or inferred; dotted where concealed 2,42 A ¥ ES a ~ ~ - A T+ Hx t 4th ~ faz aS -S el "288 Strike and dip of beds \-'¢ vas -a Sis T* Ts i% 'I\ - 90 «+7 - Strike of vertical beds rez £/%« ~ nial '" >< TRUE NORTH »Wid, Shaft 2% vay f =% % Adit L i i i i 1 1 -A WWL: & Geology by R. F. Stopper, April 1944 R. 33 E. 2000 Feet 1 FiGur® 5.-Geologic map of part of the Rawhide district, Mineral County, Nev. of feet it is in contact with the main limestone or with the overlying hornfels. Tactite bodies, however, occur only at intervals along the contact; elsewhere limestone. or marble is directly against the granite. The tactite bodies range in thickness from a few inches to 50 feet. The fresh tactite consists of andradite garnet with vari- ous proportions of calcite, quartz, amphibole, epidote, pyroxene, wollastonite, pyrite, magnetite, scheelite, and chalcopyrite. NEVADA SCHEELITE MINE The Nevada Scheelite mine consists of an inclined shaft leading to levels at 100, 200, and 300 feet, to- gether with a series of stopes between the levels. The mine is on the west side of the granite stock near a sharp bend in the contact (see fig. 5). The limestone beds at the mine strike northeast and dip from vertical to steeply southeast. A tactite body 2 to 50 feet wide occurs along the contact in an irregular zone about 1,800 feet long. In the northern and southern parts of the zone, the contact between limestone and granite is nearly vertical and mainly concordant with bedding in the limestone. - In the middle part of the zone, the contact strikes northwest and dips 30° to 40° NE., cutting sharply across the bedding. This part of the contact is believed by Stopper to follow a pregranite fault along which the beds northeast of the fault have been offset about 350 feet to the northwest. The tactite body is thickest along the middle part of the contact and is absent in places to the north and south, granite being directly against marble, The tactite in this mine 68 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES is in large part oxidized. Oxidation is marked on the 200- and 100-foot levels and extends in places below the 300-foot level, which is probably about its lower limit. Samples of tactite, granite, and marble were obtained. No systematic variation in any of these rocks was noted. The marble is in marked contrast to that associated with tactite in other contact metamorphic deposits sampled, because it contains few silicate minerals representing lower grades of metamorphism. The change from tac- tite to marble commonly is abrupt, there being no clearly defined light-colored silicated marble zone. Table 22 gives beryllia contents. Tamu 22.-Beryllia in samples from the Nevada Scheelite mine BeO Sample (percent) 329-1189 Description Chip sample across 15-ft thickness of marble beds adjoining granite, north end of drift on 300-ft level, about 540 ft north of shaft. (No tactite zone present here.). ." __. Chip sample of granite in contact with marble, north end of drift on 300-ft level, 500 to 520 ft north of shaft____. Chip sample across full width (5 ft) of tactite zone at intersection of headings about 460 ft north of shaft, 300-ft level. Chip sample across full width (30 ft) of tactite zone, stope 390, 24 to 30 ft above.300-ft level. .... Chip sample across 15-ft thickness of marble beds in west drift of 200-ft level, 200 ft northeast of shaft_______. Chip sample of marble, in part silicated (thickness, 7 ft), northeast end of main drift, 200-ft level..s.............2.L Chip sample of granite taken at intervals along face of drift, 100 to 150 ft south of shaft, 200-ft level. 0. 0008 1190 . 0007 1191 . 0028 1192 . 0024 1194 . 0004 1195 <. 0001 1228 <. 0001 HOOPER NO. 2 MINE The Hooper No. 2 mine consists of an inclined shaft 110 feet deep, a drift extending 140 feet northeast from the shaft, and a 16-foot winze that extends downward from the shaft and leads to a 20-foot drift. The work- ings follow a tactite layer in thin-bedded andalusite- biotite hornfels. The tactite layer is about 20 feet strati- graphically above the main limestone formation. Three samples taken at the mine are described in table 23. TaBus 23.-Beryllia in samples from the Hooper No. 2 mine BeO Sample Description (percent) 329-1225 Chip sample across 3-ft thickness of hornfels immediately overlying tactite, main level, north end_______________. <0. 0001 1226 Chip sample across full width (5 ft) of tactite pillar on main level___________ <. 0001 1227 Chip sample across 5-ft thickness of hornfels overlying tactite, mouth of . . . . nb camels aam m= whem s <. 0001 YANKEE GIRL MINE At the Yankee Girl mine a 40-foot adit leads to two drifts, one extending about 65 feet northeasterly, the other extending about 90 feet east-southeast. Each of the drifts is connected with the surface by a shaft. A 25-foot inclined winze leads from the floor of the east- southeast drift to a small stope. The mine is along the contact of the granite with the hornfels that overlies the main limestone unit. Inclu- sions of limestone that have been metamorphosed to tac- tite and marble are exposed in the workings. Hornfels is in contact with granite at several places in the mine. Sampling data are given in table 24. 24.-Beryllia in samples from the Yankee Girl mine BeO Sample Description (percent) 329-1229 Chip sample of hornfels 6 in. to 12 in. from contact with granite, near end of northeast drift. <0. 0001 1230 - Chip sample of granite 6 in. to 12 in. from contact with hornfels of sample 329- : 1220 ...no cae cane . <. 0001 1231 Chip sample across 5-ft thickness of horn- fels at end of northeast drift_._______ <. 0001 1232 Chip sample across silicated marble beds at and near bottom of winze_____-__. <. 0001 1233 Chip sample across tactite zone, 31 ft from end of northeast drift_________-._ <. 0001 1234 Chips from various outcrops of fresh granite from lower part of gulch below MIME... bes ss <. 0001 DESERT SCHEELITE AND GUNMETAL MINES, PILOT MOUNTAINS | -_- The Desert Scheelite and Gunmetal mines are on the east slope of the Pilot Mountains, in Mineral County. The Desert Scheelite mine is 2.4 miles S. 22° E. of Graham Spring (Tonopah quadrangle). The Gunmetal mine is about 2 miles S. 10° W. of Graham Spring. Both deposits are reached by a graded gravel road extend- ing east from Mina across the mountains. A short dis- ance east of the summit a desert road leads southward past Graham Spring and connects with the mine ac- cess roads. DESERT SCHEELITE MINE The workings at the Desert Scheelite mine consist of two opencuts, a 50-foot inclined shaft with a small stope at the bottom, a 65-foot vertical shaft, and several trenches and short adits. The workings are in an east- trending belt of interbedded gray and white marble and silicated marble. This belt contains a tabular body of tactite (see fig. 6). The rocks dip 45° to 80° N. The tactite body extends westward for 700 feet from the 65-foot vertical shaft (shaft A) and probably connects beneath covered ground with the tactite zone exposed at the surface and in the 50-foot inclined shaft (shaft B). The total length of the tactite body therefore may be more than 1,400 feet. It consists of tactite beds with irregular blocks and partings of marble and sili- cated marble. Tactite formation is controlled prima- rily by bedding, but in part its distribution is related to cross fractures cutting the marble beds. The thickness of the tactite varies markedly from place to place. LOCALITIES Bedrock concealed by gravel Bedrock concealed by gravel E-X°P L 100 0 \\;> Interbedd ed tactite and silicated Contact - , Dashed where approximately located or inferred, dotted where concealed IN NEVADA 69 seo-1240 | 1" > =q O Z Approximately located or inferred marble eo -- Strike and dip of beds Lal els ) Vertical shaft Inclined shaft. @ 329-1236 Locality sampled and number . Geology by E. N. Cameron and 200 Feet J. H. Macleod, August 1949 LEALLL AL. LL Pistol FicurE 6.-Geologic map of part of the Desert Scheelite mine, Mineral County, Nev. The tactite is fine- to coarse-grained, massive to layered rock consisting of garnet with some quartz, carbonates, and epidote. The color of the garnet ranges from red to greenish brown or yellowish brown. The mineral proportions vary locally and in places the tactite is rich in epidote. The silicated marble is main- ly a thin-bedded fine-grained rock of indeterminate composition. The marbles are gray to white, and fine grained to medium grained. The white marble evi- dently formed along bedding and cross fractures by recrystallization of gray marble. The gray marble was derived from blue-black fine-grained limestone similar to that exposed outside the tactite zone. Samples were taken as listed in table 25 and shown on figure 6. Tares 25.-Beryllia in samples from the Desert Scheelite mine BeO Sample Description (percent) 329-1236 Chip sample across full width of tactite.. <0. 0001 1237 Chip sample, bed by bed, across 15-ft thickness of marble and silicated marble directly underlying tactite, south wall of openeut :=. _._." 9. <. 0001 1238 Chip sample across full width of tactite (includes 4 ft of interbedded tactite and light silicate rock) .-..-.......... <. 0001 1239 Chip sample across full width of tactite.. <. 0001 1240 Chip sample across lower 10 ft of tactite. _ <. 0014 1241 - Chip sample across 5-ft thickness of dense thin-bedded green hornfels immedi- ately overlying <. 0001 GUNMETAL MINE The Gunmetal mine is in gently dipping tactite layers interbedded with marble and silicated marble along the contact of the beds with quartz-monzonite. The tactite beds extend as much as 100 feet from the contact. The main working consists of two adits that lead to stopes on three levels. The tactite is prevailingly garnet-rich but contains also quartz, calcite, epidote, and scheelite. A chip sample (329-1242) was taken across the lowest tactite layer exposed in an old foundation excavation north of the adits leading to the main workings. This layer is exposed for 60 feet along the strike and aver- ages 3 feet in thickness. A second sample (829-1243) was taken across the main tactite bed exposed in a wall between the mouths of two adits in the first stope of the main workings.. The samples showed no BeQ, the limit of sensitivity being 0.0001 percent. MANGANESE-TUNGSTEN DEPOSIT AT SODAVILLE The Sodaville manganese-tungsten deposit, also known as the Black Jack claim, is on a pediment about half a mile west of U. S. Highway 95 opposite the former railroad station at Sodaville. The deposits are mostly on the crests and flanks of two small knobs that rise above the pediment. They have been described by Kerr (19462, p. 178). The deposits are veins in two steeply dipping north- to northeast-trending fracture zones cutting cherty rock that forms the knobs and underlies the pediment. The richest veins are on the eastern knob and the ad- jacent part of the pediment. They range from less than 1 inch to 2 feet in width and are as much as 20 feet in length. The veins consist largely of tungsten- bearing psilomelane, with varying amounts of pyro- lusite, wad, iron oxides, calcite, gypsum, quartz, and chalcedony. The tungsten content of the psilomelane is reported to be 4.88 percent (Kerr, 1946a). Reserves 70 are small, and operations at the deposits have never gone beyond the prospecting stage. For comparison with the larger deposit at Golconda, a chip sample (329-1235) of high-grade manganese- tungsten ore was taken from blocks on various small ore piles. It contained 0.0075 percent of BeQ. ANDALUSITE DEPOSITS NEAR THORNE The andalusite deposits that are exposed on both edges of the Soda Spring Valley a few miles east of Thorne, Mineral County, occur in a belt about 7 miles long that traverses the lower foothills of the Gillis Range (Hawthorne quadrangle). Another andalusite deposit is exposed at the Deep mine, a prospect on the southeast side of a prominent knoll immediately south of Highway 95, about 8 miles east-southeast along the highway from the center of Hawthorne. Two deposits on the south edge of the Gillis Range, the Green Tale mine and a mine of unknown name about 0.4 mile west-northwest of the Green Tale mine, were visited and sampled. GREEN TALC MINE The Green Tale mine is on the lower southeast end of a spur of the Gillis Range. The mine consists of three opencuts and a series of prospect pits scattered over an area about 500 feet long and 125 feet wide, trending northeast across the spur. The main working, rear the southwest end of the area, is an opencut 100 feet long, 90 feet wide, and about 40 feet in maximum depth. At the northeast end of the area is a second opencut about 45 feet long, 45 feet wide, and 25 feet in maximum depth. A third, small opencut is immediately north of the main opencut. The principal body of andalusite-bearing rock appears to be the one exposed in the main working. The core of this body strikes N. 5° W. across the opencut and is more than 125 feet in exposed length and 10 to 15 feet thick. It is exposed to a maximum depth of about 12 feet and appears to dip steeply east. The core consists principally of 10 to 50 percent andalusite in blue to lavender crystals and clusters of crystals %% inch to 1 inch in diameter and 14 inch to 4 inches long, set in a green to brownish-green matrix of pyrophyllite. The andalusite crystals are stout, rounded prisms apparently showing marginal alteration to pyrophyllite. In places a brownish granular material, possibly a carbonate, is present in the greenish matrix, and locally this is the dominant constituent. Enveloping the andalusite-bear- ing rock is a variety of altered volcanic rocks. The northeast cut exposes dark volcanic rocks irregu- larly altered to pyrophyllite, with varying amounts of OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES the brown granular mineral. Irregular bodies of simi- lar pyrophyllitic rocks are scattered over the crest of the hill between the northeast opencut and the main working. The largest of these bodies appears to be about 50 feet long and 20 feet wide. Samples taken at the Green Tale mine are described in table 26. TaBum 26. -Beryllia in samples from the Green Tale mine BeO Sample (percent) 329-1197 Description Chip sample across 10-ft thickness of pyrophyllite-carbonate(?) rock, north- east wall of lower part of northeast opencut, above layer of dark, altered voleanie rock. Chip sample across 10-ft layer of dark altered volcanic rock, underlying rock of sample 329-1197. _ .______________ Chip sample across full width (8-10 ft) of andalusite-bearing core rock. Small opencut north of main working...... Chip sample across full width (15 ft) of andalusite-bearing core rock, north wall of main working.. <0. 0001 1198 <. 0001 1199 <. 0001 1200 <. 0001 MINE NEAR GREEN TALC MINE 'An unnamed mine 0.4 mile west-northwest of the Green Tale mine consists of a glory hole about 60 feet in diameter and about 60 feet in maximum depth. On the southeast side of the pit there is a vertical shaft re- ported to be about 75 feet deep. The mine is in a lens of andalusite-pyrophyllite rock that strikes N. 65° E. and is nearly vertical. The lens is about 40 feet in maximum width and its strike length is probably not much more than 60 feet. On its north- west side the lens appears to grade irregularly into altered volcanic rock, and on its southwest side it is cut off by a steeply southeast-dipping, gouge-filled fault zone. Chip sample 329-1224 was taken across an andalusite- bearing lens exposed in the southwest wall near the bottom of the glory hole. It showed no BeQ, the limit of sensitivity being 0.0001 percent. NYE COUNTY GABBS AREA We spent one day near Gabbs, Nev., sampling de- posits of scheelite, magnesite, and brucite. The main purpose of the visit was to sample the scheelite-leuch- tenbergite vein in the Paradise Range described by Kerr and Callaghan (1985). Examination revealed, how- ever, that the vein is poorly exposed and probably of small tonnage; consequently no samples were taken. The newly developed Victory tungsten deposits were examined and sampled. A few samples were taken at the mine of the Sierra Magnesite Co. and from the brucite deposits at Gabbs. LOCALITIES IN NEVADA TIL VICTORY TUNGSTEN DEPOSITS The Victory tungsten deposits are in the northwest ern part of the Tonopah quadrangle and on the south- west slope of the Mammoth Range about 3 miles west- southwest of Marble. They are in the north part of sec. 22, T. 13 N., R. 36 E., and are accessible by a dirt road that turns northeast off State Highway 28 at a point about 1 mile northwest of the Gabbs airport en- trance road. The deposits are on the crest and north- east side of a spur and are at the west border of a north- ward-trending body of granodiorite. The granodiorite mass is probably more than a mile long and is at least a quarter-mile wide. The deposits are of two types: disseminated scheelite in granodiorite, and scheelite- bearing contact-metamorphosed calcareous rocks. Deposits of the first type are exposed in a series of 5 trenches 30 to 75 feet in length. The surface slopes 22° E. and the trenches extend for about 250 feet along a line that trends northwest. The trenches are excavated in a medium- to coarse-grained biotite granodiorite lo- cally containing streaks and patches of quartz. Exam- ination by ultraviolet light shows that scheelite is dis- seminated through the rock, but the content varies markedly from place to place. A chip composite sam- ple (329-1248) was taken along 57 feet of the second trench (counting from north to south along the line of trenches) and 37 feet of the third trench,. Spectro- graphic analysis showed 0.0034 percent BeO in the sample. The second type of deposit is exposed west of the first, in a series of trenches at and near the crest of the same spur. The trenches are 15 to 30 feet in length and are spaced at intervals along a line trending northeast for at least 200 feet. They expose an undulating contact of granite with limestone and quartzite. At the crest of the spur the contact is nearly horizontal, but it ap- pears to dip west where exposed on the west side of the spur. Along parts of the contact where limestone abuts against granite, a zone of silicated marble 6 inches to 2 feet thick is present. The minerals present include biotite, chlorite, and possibly amphibole and pyroxene. In the two southernmost trenches a well-exposed con- tact zone, according to local report, contains the best showing of tungsten along the west contact of the gran- odiorite. A chip sample (329-1249) of the contact- metamorphosed material was taken along the 25-foot length of the southernmost trench and was found to contain 0.014 percent BeO. In view of the relatively high beryllium content of this sample, further study of the deposit seems advisable. BRUCITE AND MAGNESITE DEPOSITS The brucite deposits at Gabbs are on the west slope of the Paradise Range, east of town. They are being worked by the Basic Refractories Co. The work- ings consist of two series of large irregular opencuts, one in an upper deposit, the other in a lower one. The workings visited are in the upper deposit. They have a maximum depth of more than 350 feet and extend along the strike of the deposit for about 800 feet. The deposits are in a thick series of magnesite and dolomite beds along the contacts of a northward-pro- jecting prong of a granodiorite stock. The brucite formed by hydrothermal alteration of the carbonate rocks. Irregular masses of dolomite and magnestite in various stages of alteration are contained in the brucite. The deposits are capped by blankets of supergene hy- dromagnesite that are as much as 50 feet thick. The whole assemblage of dolomite, magnesite, and brucite is cut by an intricate network of granodiorite dikes, each bordered by serpentine. The high-grade brucite is compact and appears soapy. It grades into rock locally called "limy brucite" that contains much dolo- mite and calcite. Two grab samples of the brucite were obtained from the lower level workings of the east (upper) ore body. Sample 329-1245, high-grade brucite, contained less than 0.0001 percent BeQ; sample 329-1246, limy bru- cite, contained 0.0014 percent BeQ. The extensive deposits of magnesite in this area have been described by Rubey and Callaghan (Hewett and others, 1936, p. 142-143). A sample (829-1244) of raw magnesite obtained from the crusher at the mine of the Sierra Magnesite Co. contained less than 0.0001 percent BeQO. PERSHING COUNTY ROCKS IN THE WEST HUMBOLDT RANGE The West Humboldt Range is noteworthy for the association of scheelite and beryl in two deposits on the west slope of the range-the Humboldt Canyon beryl- scheelite prospect and the Oreana tungsten mine, With the idea that these deposits might indicate the presence of an unusual amount of beryllium in one or more of the several types of granitic intruded rocks exposed in the range or in the contact-metamorphic rocks border- ing them, a fairly extensive program of sampling was undertaken. | LIMERICK CANYON AREA Large masses of aplite have been described by Knopf (1924, p. 33) and Jenney (1985, p. 34, 35) from the Rochester mining district and the area immediately north of it. The aplite is a fine-grained massive rock that, according to Jenney, consists mainly of quartz, orthoclase, and albite, with traces of magnetite, sphene, tourmaline, zircon, and biotite. No exhaustive study of the aplite was attempted, but T2 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES two samples were taken from exposures in Limerick Canyon (see fig. 7), as follows: 329-1126. Chip sample from various exposures on the north side of Limerick Canyon (0.0007 percent BeQ). 1127. Chip sample from various exposures on the south side of Limerick Canyon (0.0011 percent BeQO). TRUE NORTH s After Jenney, 1935, pl. 1 2080 (l) 4000 Feet T 1 1 l Contour interval 200 feet Datum is mean sea leve! EXPLANATION 1% _ (t f +t }§§ Contact 2s ) ar Alluvium d } t Fault I7 Em - 23 £ Granite porphyry 08 329.1126 au + <4 H e. Locality sampled + /+ C to and number A- 3 ac Aplite ASM 9 w w 4. Keratophyre LE FrGurE 7.-Geologic map of part of Limerick Canyon, West Humboldt Range, Pershing County, Nev, Dikes of granite porphyry cut aplite on the south side of Limerick Canyon (fig. 7). Sample 329-1128 con- sisted of chips from various exposures of five dikes. The BeO content proved to be less than 0.0001 percent. This same rock forms large bodies in the area extending north from the Rochester mining district toward Unionville Canyon. PANTHER CANYON AREA The Panther Canyon area has been described by Vitaliano (1944). In Rye Patch Agnes Canyon quartz monzonite underlies an area of 20 acres, and contact-metamorphosed rocks associated with it under- lie large parts of an area 2,400 feet by 3,200 feet, extend- ing from the south side of Rye Patch Agnes Canyon across Panther Canyon (see fig. 8). Because Vitali- ano's report includes detailed maps of both the intrusive body and the associated contact aureole, the area ap- peared to offer excellent ground for sampling. The quartz monzonite is a light-gray medium-grained massive rock reported by Vitaliano to consist mainly of quartz, feldspar, and mica, with accessory sphene, apatite, magnetite, and pyrite, and traces of epidote, calcite, hematite, chlorite, and zircon. It is finer grained than the granite in Rocky Canyon (fig. 11) and con- tains more plagioclase. The quartz monzonite shows little variation. At a few places it grades into aplite. Outerops of the quartz monzonite along Rye Patch Agnes Canyon were carefully examined, for beryl and for indications of uncommon minerals. A chip sample of granite (329-1124) was taken from outcrops at 15- foot intervals along the bottom of Rye Patch Agnes Canyon, from the east contact nearly to the midpoint of the granite body. The sample contained 0.0016 per- cent BeO. Two principal groups of rocks have been affected by contact metamorphism in the Panther Canyon area: calcareous argillite, now represented by hornfels lay- ers; and limestones, ranging from pure to argillaceous and including thin layers of argillite. The hornfels is mainly represented by three layers of a brownish (limonitic) sugary textured rock from 6 to 50 feet in width. The easternmost layer was sampled (329-1123) on the north side of Rye Patch Agnes Can- yon just above the canyon bottom. At this point it is about 45 feet thick. The rock consists largely of quartz and orthoclase, with subordinate amounts of diopside, epidote, and other minerals The sample contained 0.0008 percent BeQO. The limestone layers are an extremely varied assem- blage, ranging from blue-black, fine-grained marble that apparently has undergone recrystallization but lit- tle silicification, through blue-black marble containing streaks and patches that range from white marble and silicated marble to tactite. Metamorphosed limestone occurs mainly in two zones: an inner zone immediately contiguous to the quartz monzonite in Rye Patch Agnes Canyon, and an outer zone east of this body and, ex- tending roughly north from the south side of Rye Patch Agnes Canyon across the south fork of Panther Canyon (see fig. 8). In the inner zone, silicification of the limestone series is only locally complete and the rocks consist largely of blue-black marble with streaks, patches, lenses, and lay- LOCALITIES IN NEVADA (% +. AY .+ Ifi‘flN yas Pa S¥Pzs o x f Contour interval 100 feet Datum is mean sea level 78 EXPLANATION SEDIMENTARY ROCKS Alluvium and slope wash is Calc hornfeis N Ch. s : Metamorphosed limestone Metadiorite 4. Contact Limestone Dashed where approximately located or inferred IGNEOUS ROCKS + u wemon mance <1 l+ 0d." D 3 n.3.. % Fault Rhyolite Dashed where approximately located or inferred; U, up- thrown side; D, downthrown After Vitaliano, 1944, fig. 2 20|00 Feet 18°30 / . " side m Quartz veins m & x 55 6 § G Tobe a| /o CZ Strike and dip of beds A "ZI /£ a El [# Camptonite s Freur®E 8.-Geologic map of a part of Panther Canyon area, Rye Patch, Nev. ers of white marble and silicated marble. Samples taken and analyzed for BeO are described in table 27. TaBur 27.-Beryllia in samples from inner contact zone, Panther Canyon area BeO Sample Description (pagan!) 329-1111 Chip sample taken at intervals across a series of thin layers of silicated marble intercalated with marble. Zone is 40 ft across strike and 200 ft long.._______ < 0. 0001 1112 Chip samples across zone of interbedded gray, white, and blue-black marble containing layers of silicated marble. Total thickness of zone is 54 ft; 18 ft is silicated marble (329-1112) and 36 ft is marble . 0078 1118). ___. do re peels ine alde dae bac a a ae ales . 0013 1122 Grab sample of tremolite marble from limestone area north of quartz monzo- 2. . 4222 ee oto - =a an inks ie a . 0013 1125 Chip sample from various outcrops of blue-black marble containing patches of white marble and veins of silicates.. . 0016 The outer contact-metamorphic zone includes rocks that are thoroughly silicated. These rocks range from hornfels and silicated marble to tactite and can best be seen in the ridges separating the North and South forks of Panther Canyon. The section exposed on the north wall of the south fork is typical (fig. 9). The structure of the outer zone is complicated by a steeply dipping fault that marks the eastern margin of the zone, at least between the North and South Forks of Pan- ther Canyon (fig. 10), and there may also be one or more faults along the bottom of the south fork of the Streaked gray and white silicated marble 15 feet thick * Unaitered - , limestone 329-1118 Sample number Contact Dashed where approx mately located or inferred White marble zone 140 feet thick __ FIGURE 9.-Sketch of part of north wall, South Fork Panther Canyon, Pershing County, Nev. T4 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES canyon. Sampling was restricted largely to the north wall of South Fork Panther Canyon, west of the fault ; sampling data are given in table 28. TaBu® 28.-Beryllia in samples } from outer contact zone, Panther Canyon area BeO Sample Description (percent) 329-1115 Chip sample across belt of silicated marble, north side Rye Patch Agnes aus tlie s 0. 0007 1116 Chip sample across beds approximately 15 ft thick in lower part of section of gili¢ated . 0009 1117 Chip sample across tactite zone, taken along crest of ridge.............1_._. . 0037 1118 Chip sample across beds of hornfels__.__. . 0026 1119 Chip sample across 15-ft thick zone of sflitated . 0029 1121 Chip sample across 140-ft thickness of beds, mostly . 0036 1 Samgles 320-1116 to 329-1121 are from the section on north side of South Fork of Panther Canyon. See figure 9 for locations. ROCKY CANYON-WRIGHTS CANYON AREA The area extending from Rocky Canyon to Wrights: Canyon includes the Oreana tungsten mine, described by Kerr (1938; 1946a, p. 189-192), where scheelite and beryl occur in pegmatite. The general geology of the area is shown in figure 10, and detailed geology in the vicinity of the Oreana mine is shown in figure 11. The rocks sampled include limestone in various stages of recrystallization and silicification, hornfels, granite and aplite. Locations of samples are shown on figures 10 and 11, and sampling data are given in table 29. Tasur 29.,-Beryllia in samples from the Rocky Canyon-Wrights Canyon area BeO Sample Description (percent) ROCKY CANYON AREA 329-1130 Chip sample across pegmatite-aplite dike, north side of 0. 0001 1131 - Chip sample of aplite from composite dike on south side of __. . 0011 1132 Chip sample of granite; chips taken at 150-ft intervals for 4,000 ft up canyon from o . 0011 1133 Composite sample of six pegmatite-aplite dikes, north side of canyon-____.____._. . 0007 1135 Chip sample of granite; chips taken at intervals along ridge south of canyon.. . O01 WRIGHTS CANYON (OREANA) AREA 329-1137 Chip sample across aplite dike_________. . 0011 1138 Chip sample across hornfels layer______. . 0008 1139 Chip sample across aplite dike or sill___. . 0015 1140 Chip sample across lens of silicated marble and tactite between aplite dikes.... . 0031 1141 Chip sample across silicated marble. ._... . 0015 1142 Chég sample across aplite dike, north side rights . OO1 The granite is exposed in the gorge forming the lower part of Rocky Canyon. It is a medium- to course- grained massive biotite granite. Apart from patches of biotite-rich material present locally, particularly near the mouth of the gorge, it appears homogeneous. After Jenney, 1935, pl. 1 OREANA TUNGSTEN MME ls] 2000 4000 Feet L0 4-3 T 1 as..) Contour interval 200 feet Datum is mean sea leve! SEDIMENTARY AND exFLANATION METAMORPHIC ROCKS Contact Dashed where approximately located ERNARY i U p Middle Triassic _ Recent TRIASSIC Fault Dashed where approximately located; dotted where concealed; U, upthrown side; D, downthrown side Limestone and marble IGNEOUS ROCKS ~- Sh Pliocene erma 1. .. i Strike and dip of beds TERTIARY A Diabase Lal Shaft 329-1133 & Pegmatite or quartz vein T< <> ah wan 329-1135 _ 3 \ PES] - Locality sampled and number Granite + 0+ + + +04 % +040 % Aplite JURASSIC AND CRETACEOUS(M) 9 * z = a Z 4 } } | s } Diorite TRUE NORTH sic Ar camel Middle(?) TRIASSIC L Rhyolite FiGeurE 10.-Geologic map of part of Rocky Canyon and vicinity, West Humboldt Range, Pershing County, Nev. The granite was examined for beryl, but none was found. Aplite-pegmatite dikes are found in great profusion. Proportions of aplite and pegmatite material in the dikes vary markedly, even from place to place within the same dike, but the aplite fraction predominates. In general the dikes strike N. 30° to 45° W. and dip 35° to 50° NE.; some strike northeast and are vertical. They range from a few inches to many feet in width, and some are exposed for hundreds of feet along strike or dip. Apparently, they are of several generations and some of the older are sill-like bodies in rhyolite LOCALITIES IN NEVADA T0 4 ge // AD u7/)/‘ Tanr yor gen ut AQ<\ 0/1 Nis a aii = ,,__V~~.\/_—H///' 3 £ ; m"" Z &, x 4 4 ly \ =q I \ U . b AW As /"\\ Sf Adapted from map by Kerr, 1946a, pl. 7 500 0 ; 1000 Feet {+. ( Le ja | 1 ] EXPLANATION 7 o S -g T GrZ ”5;22;5/ x \\|//\\” * >'\/\|\\ 123 xe .~. r eA - Marble Limestone and Hornfels Aplite Older aplite Metadiorit Granite marble and rhyolite LOCALITY AND SAMPLE NUMBER 3 1. 329-1137 4. 329-1140 w s -' © 2. 3zo-1138 5. 329-1141 Contact Fault Localities sampled 3. 329-1139 6. 329-1142 Dashed where approximately located or inferred Dashed where approximately located FigUrE 11.1-Geologic map of vicinity of Oreana tungsten mine, Pershing County, Nev. 76 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES (Kerr, 19462, p. 189-190, pl. 7). Beryl was not found in the dikes examined. In the area east of the Oreana mine, contact-meta- morphosed rocks consisting of blue-black limestone and marble, silicated marble, tactite, and hornfels were sam- pled. These rocks are in contact with metadiorite on the west and granite on the east (see fig. 11). RESULTS OF SAMPLING In view of the occurrence of beryl in scheelite de- posits in the West Humboldt Range, analytical results of the rock samples collected in this region are disap- pointing. Of the 27 samples of all rock types that were analyzed spectrographically, only 1 (329-1112) con- tained more than 0.005 percent BeQ, and only 3 others contained more than 0.003 percent. The average BeQO content of the other 23 samples is less than 0.002 percent. Sample 329-1112, containing 0.0078 percent BeQO, rep- resents material which might some day be of commer- cial interest, though the tonnage probably is small. The sample is from a zone of silicated marble adjacent to the intrusive quartz monzonite in Rye Patch Agnes Canyon. The zone is more than 50 feet wide and per- sists for at least 200 feet along the strike. It is esti- mated to contain about 3,500 tons for each 10 feet of depth. The beryllium-bearing mineral is not known, and there is no assurance that the beryllium is recover- able. In evaluating results of the sampling, it should be emphasized that the metasedimentary rocks at each of the localities sampled in the Humboldt Range are of extremely diverse composition. Hundreds of samples, each taken from a single bed, would be needed to de- termine the exact distribution of beryllium. Consider- able contamination is inherent in the present sampling; thus further investigation might reveal material of much higher beryllium content than that indicated by the analyses given above. However, the present work gives no indication of large individual deposits of rela- tively high-grade beryllium-bearing material. TUNGSTEN AREA, MILL CITY DISTRICT The tungsten deposits at Tungsten, near Mill City, Nev., are among the most important of the tactite type in the United States. The deposits, which are worked by the Nevada-Massachusetts Co., are on the southeast slopes of the Eugene Range, in Pershing County. They have been described by Kerr (1946a, p. 182-188). At Tungsten three steep-sided stocks of granodiorite cut a series of calcareous strata interbedded with horn- fels. In general the beds strike nearly north and dip steeply east or west. The beds are offset by both pre- and post-mineralization faults. The deposits are in parts of the calcareous beds that have been converted to tactite and impregnated with scheelite. Scheelite- bearing tactite has been found in some of the beds for distances as great as 2,000 feet from the nearest in- trusive body, and the deepest workings have reached 1,700 feet without sign of bottoming of the beds against granite. No one of the calcareous beds is uniformly mineral- ized. In general, a bed traced along dip or strike will be found to show four facies, as follows: 1. Tactite, consisting chiefly of garnet, epidote, diopside, and quartz in various proportions. 2. Silicated marble, with pale-green silicates and pale garnet. 83. White marble, commonly with some light-colored silicates and grading in places into silicated marble. 4. Blue-black fine-grained marble grading into limestone. Cer- tain beds contain partings or lenses of hornfels. The number of calcareous beds is large and the work- ings are extensive; no attempt at overall sampling could be made. Two groups of beds, known locally as the Sutton beds and the George beds, were selected for the major part of the sampling, because each was easily accessible in several opencuts. A few samples were also taken from beds on Humboldt Hill and Stank Hill. The various ore-bearing beds and surface work- ings are shown on figure 12. None of the samples from this area contains sufficient beryllium to be of commercial interest at present. In view of the large number of samples taken and the va- riety of rock types represented, the prospect that sub- stantial quantities of higher grade material is present seems unlikely. f SUTTON BEDS OF LOCAL USAGE The rocks known locally as the Sutton beds consist of two calcareous layers separated by about 40 feet of hornfels. Samples were taken from these beds in the Baker workings, the workings immediately north of the Springer stock, and the south opencut of the Sutton mine. The samples are described in table 30. Tasu® 30.-Beryllia in samples from the Sutton beds of local usage BeO Sample Description (percent) EAST SUTTON OPENCUT; EXPOSURES IN LOWER PART OF HEADWALL (NORTH WALL) 329-1143 Chip sample, layer by layer, across east ore bed, thickness 9 to 9.5 ft. Inter- banded tactite, white marble, silicated marble, quartz, and hornfels. Tactite includes both garnet-rich and epidote- rich material. 1144 Chip sample of west ore bed, 8.5 ft thick. Garnet-epidote-quartz-calcite _ tactite with minor hornfels layers_._._______._. 1145 Chip sample of blue-black and gray horn- fels from 40-ft thickness of beds sepa- rating the two ore beds_____________. Chip sample from same beds as 329-1145 but consisting of hornfels altered along <0. 0001 . 0017 . 0016 1146 layering and cross fractures to a green fine-grained rock....-._-_.._..._...... . 0012 LOCALITIES IN NEVADA 7T. Tasur 30. -Beryllia in samples from the Sutton beds of local usage-Continued BeO Sample Description (percent) EAST SUTTON OPENCUT; EXPOSURES IN LOWER PART OF HEADWALL (NORTH wart) -continued 329-1147 Chip sample across 6 ft of hornfels im- mediately overlying the west ore bed.. 1148 Chip sample of 4 ft of hornfels immedi- ately underlying the east ore bed.... 0. 0018 <. . 0001 soUTH SUTTON OPENCUT; EXPOSURES IN LOWER PART OF HEADWALL (SOUTH WALL) 329-1149 Chip sample across east ore bed, 44 in. thick at base of cut. Mostly marble and silicated marble, with some tactite. Chip sample of hornfels separating the two ore beds; thickness about 41 ft... Chip sample across west ore bed, 9 ft thick at base of cut; gray marble, and silicated marble, with inclusions of blue- black marble, garnet-rich and epidote- rich thctito 's uds Chip sample across 6 ft of hornfels im- mediately overlying (west of) the west Ore bed.. .... scc d-. . cl 00 ohn a iaa apie nn Chip sample across 4 ft of hornfels im- mediately beneath (east of) the east ore bed c... c..... lsu se - ee Grab sample of the blue-black marble from broken material near the north end of the openeut..._.....s._...._... . 0025 & O01 1150 1151 . 0032 1152 . 0013 1153 . 0013 1154 0006 OPENCUT EAST OF BAKER WORKINGS; EXPOSURES AT BASE OF HEADWALL. (THE CORRELATION OF THESE BEDS WITH THE SUTTON BEDS OF LOCAL USAGE IS UNCERTAIN.) 329-1155 Chip sample across west ore bed, about 5.5 ft thick. Consists mostly of sili- cated marble containing garnet. In- cludes 2 ft of blue-black marble and gray Jans 329-1156 Chip sample across east ore bed, about 15 ft thick. Upper half mostly diopside- epidote rock and garnet rock. Lower half mostly fine-grained to medium- grained marble_._........__._.__....- . 004 . 0029 BAKER WORKINGS]; EXPOSURES IN ENTRANCE CUT AND soUTH WALL OF OPENCUT Chip sample across west ore bed, 125 ft thick. Consists mostly of dense, light- green cale-silicate rock. Upper 2 ft is garnet Chip sample across 6 ft of hornfels im- mediately adjacent to west (hanging) wall of west ore Chip sample across east ore bed, 5 ft thick. Mostly epidote-rich - tactite veined by quartz. Chip sample across 4-ft thickness of horn- fels forming east (foot) wall of the east ore body..1 . ce} wane witn in ale haine in Chip sample across an aplite dike cutting the ore beds and enclosing hornfels in the south part of the opencut. The dike strikes N. 55° W. and dips 77° SW. 1It; is 6 to 15 ft thick and at least 100 ft .. L in - Shs ts bow aaa «nano 1162 Chip sample across 40-ft thickness of hornfels separating the two ore beds.. 329-1157 . 0027 1158 . 0023 1159 . 0026 1160 . 002 1161 . 0008 . 0012 ©PENCUT NORTH OF THE BAKER WORKINGS; EXPOSURES IN SOUTH END OF OPENCUT 329-1163 Chip sample across east ore bed, 2% ft thick. White and blue-black marble, silicated marble, and epidote-garnet- quarts . 0022 1164 Chip sample across west ore bed, 26 in. thick. Epidote-quarts and garnet- quarts . 003 GLORGE BEDS OF LOCAL USAGE The rocks known locally as the George beds are a varied assemblage of layers of marble, cale-silicate rocks, and tactite composed of diopside, garnet, and epidote in various proportions. In part the diopside- garnet rocks appear to have been formed by alteration of dark-gray hornfels, not of limestone. This is clearly shown in workings 2,000 feet north-northwest of the summit of Humboldt Hill. Here the George beds are about 19 feet thick and nearly vertical. They consist of garnet-diopside tactite, grading into hornfels, and blue-black marble partly recrystallized to white marble. Samples from the George beds are described in table 81. TaBus 31.-Beryllia in samples from the George beds of local usage tip € Sample Description (percent) SHALLOW CUT ON SADDLE NORTHWEST OF sUMMIT OF HUMBOLDT HILL 329-1165 Chip sample across lower (east) part of beds, consisting, from east to west, of (1) garnet-quartz-epidote tactite 14-21 in. thick; (2) interlayered gray-green cale-silicate rock, hornfels, and fine- grained tactite, 32-40 in. thick; (3) in- terlayered hornfels and cale-silicate rock 32 in. thick; (4) garnet-rich and 3 epidote-rich tactite 71 in. thick.____--. 1166 Chip sample of beds overlying beds of 329-1165: (1) white marble, in part silicated, containing blocks of blue-gray marble, 85 in. thick; (2) garnet tactite 3-12 in. thick; and (3) white and blue- Black 1167 Chip sample of upper beds, comprising (1) garnet and garnet-epidote tactite, 33 in. thick; (2) garnet and garnet- epidote tactite interbanded with gray- green cale-silicate rock, 12-16 in. thick; (3) garnet and garnet-epidote tactite, 30 in. thick, and (4) fine-grained green cale-silicate rock, 12 in. thick.___----- 0. 003 . 0008 . 0013 OPENCUT IN GULCH ABOUT 1,500 FEET WEST OF sUMMIT OF HUM- BOLDT HILL; EXPOSURES IN LOWER PART OF SOUTH FACE OF CUT 329-1172 Chip sample across (1) 21 in. of inter- banded gray hornfels and diopside(?) hornfels, with a few thin garnet bands; (2) 25 in. of interbanded diopside(?) and garnet tactite, and (3) 9 in. of dense green cale-silicate 1173 Chip sample across 3.5-ft thickness of blue-black marble in large part con- verted to white marble, partly silicated . 1174 Chip sample across 6.5 ft of diopside and diopside-quartz rock, with thin garnet j layers and lenses_____-__------------ 1175 Chip sample across 6 ft of hornfels imme- diately east of the George beds of local Uusagel:____-!l __ _JL..L:.. ske . 0021 . 0007 . 0026 . 0016 OTHER ROCKS SAMPLED The Humboldt beds of local usage were sampled in the opencut near the summit of Humboldt Hill where they have a total thickness of about 13 feet. The beds comprise epidote-quartz and garnet-quartz tactite, sili- 78 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TFs 7 s mS NE n on o moar vey (Ans "8 a' n SN So I a o ne iy 154 * 355, is SVZ a § n ## th \\\-" «7 un = a - r (ny > s "s a2 P 3 George beds of local usage ss <2 M $ A W {George bels of If d [4 Nocal ugage,_ {it Sutton beds of local usage 704 EXPLANATION L& Alluvium and slope wash al 559 a 5 P Hornblende andesite F suant E #a.*= , 3 a le a J & Granodiorite Sin» e Limestone g ta» Silicated limestone TRIASSIC TH SUTTON MINE e Mainly hornfels z - Contact Dashed where approximately located or inferred w- _-_ Fault Dashed where approximately located or inferred wh Strike and dip of beds syrron agi OPENCUT SOUTH SUTTON SYTTON OPENCUT GuLCH 6“ 4 Contour interval 250 feet Datum is mean sea level 20100 Feet FiGurE 12.-Geologic map of part of Tungsten area near Mill City, Pershing County, Nev. cated marble, white marble, and blue-black marble. The beds on the west side of Stank Hill were sampled in the hope of getting representative material from the outer fringes of the mineralized area. Samples from these localities are described in table 32. TaBur 32.-Beryllic in samplisr {70m Humboldt Hill and Stank 7 4 32.-Beryllia in samples from Humboldt Hill and Stank Hill-Continued Description BeO Sample (percent) BEDS WEST OF STANK HILL 329-1176 Chip sample of 6-ft thickness of argillite immediately east of (overlying) the ore bods. ._.}. se ee une 42 eae s ll L. 1177 Chip sample across 32 in. of silicated marble and 30 in. of interbanded diop- side and garnet tactite. These beds per 0. 0023 BeO Sample Description (percent) HUMBOLDT BEDS OF LOCAL USAGE; OPENCUT ON HUMBOLDT HILL 329-1168 Chip sample across the full width of the Beds -s > 2 H >o a n gL MH nea de mnen anal . 0. 0033 1169 Chip sample of 5-ft thickness of hornfels immediately beneath (east of) the ore . 2 ! 2228 cee Lal Pan on aie ante a i . 0014 1170 Chip sample from various layers of garnet 222 c erly pud ae a Lan ne ne nea all ., . 0036 1171 Chip sample of white marble having abundant pale garnet________________ . 0022 form the top (east) part of the main zone of calcareous strata__._____.___ a. 1178 - Chip sample across 6-ft thickness of blue- black and white marble and silicated marble forming the middle part of the main zone of calcareous strata________ 1180 Chip sample across 4%%-ft thickness of hornfels overlying (east of) the main zone of calcareous strata and separat- ing them from 2.5 ft of blue-black and white . 0016 . 0005 . 0014 / LOCALITIES A. composite (329-1181) of granodiorite from vari- ous outcrops in the southwestern part of the Springer stock had a BeQ content less than 0.0001 percent. ROSE CREEK MINE The Rose Creek tungsten mine is in the northeastern part of the East Range, 11 miles south-southwest of Winnemucca. A detailed study of the deposit was made by R. J. Roberts (1943). Rocks of the area in- clude dolomite, limestones, argillite, and quartzite which have been cut by a small granite body (see fig. 13). Argillite next to the granite has been altered to horn- fels, and tactite has formed in the limestone. The main, or upper, workings consist of an adit that extends westerly for about 400 feet and connects with a series of drifts, raises, and stopes (see fig. 14). An inclined winze extends down the ore bed to the north- west. A lower adit was driven westerly from a point After R. J. Roberts, A. E. Granger, and M. W. Cox (Roberts, 1943, pI. 2) 250 s o 1000 Feet T L T 1 Contour interval, 100 feet Datum is mean sea level: Approximately located or inferred 79 370 feet northeast of, and 117 feet lower than, the portal of the upper adit to intersect the winze (fig. 13). This adit was flooded at the time of the present in- vestigation. A sublevel consisting of a few short drifts was excavated after Roberts' survey. It joins the winze about 35 feet vertically below the upper adit. The deposit is a bed of scheelite-bearing tactite en- closed in interbedded quartzite and hornfels. The bed is 2 to 4 feet thick, averaging about 214 feet. The aver- age thickness of the parts of the bed remaining in the underground workings is probably 114 to 2 feet. The bed strikes northeasterly and dips northwesterly at a moderate angle. It is offset by a number of postmin- eralization faults, mostly of small displacement, and is cut by preore lamprophyre dikes and postore diabase dikes. Mining has been confined to the richer and thick- er parts of the bed. The tactite is fine grained and is composed chiefly of IN NEVADA EXPLANATION FA wow cree 1 Lui E ( Fault f < < Dashed where approximately located * - 2 Z or inferred; dotted where concealed Alluvium jo E | fea Thrust fault [e] E T, upper plate U 30 Basic dike = < Pug y s 8 >- Strike and dip of beds s ial o B& so rosita t p- % =- atric l; Strike of vertical beds Granite ) _ 60 p Strike and dip of joints w & Lal //J Mine shaft Limestone ; o & Pit or trench u 329-1105 Silicated marble a Locality sampled and number < m i- Argillite and quartzite A \\\\\§\\§\ san Dolomite Tactite bed ~ Contact - FIGURE 13.-Geologic map of the Rose Creek mine and vicinity, Pershing County, Nev. - 80 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES \ \ TRUE NoRTH e K rer N Tals 6+. ~ ~ 2% ~a 320-1099 x2 % Lower Iimkit of stope not known P 20 7? I y Cayilis _ raise 1 / Wp seo-1102 sro-1104 320-11009 / Dike contains scheelite ___ 4 " 4 T a le in fissures es S C \ ///’4 pF lle ft)“. 320-1103 dig WX / Ni‘wu & AB comment yy > % Ista AS u U 7 p A Asi Lo . Atty, 07 / Wp o 8s MM f. Mum 47, 4 » ** | P { "ny ty ip, I Z , \/ ** # aA / 523i: 3 verer anit "4 % f 3 2 at Tf 1 s C < Ore bed t ¢ S ‘Dfl’nflzrf’ 1};’7',',,’;y|..,”” El. 4994 ft § S re bed largely epidote Trace of ore bed on "wl lu 00k E T T IMM sjs and calcite the surface "m intimin oof & mmm een 3 "bo EXPLANATION Sparse scheelite in Dike cuts off ore _ IU2TtZ veinlets HSIHSD # # bed in raise ap «# th 6, Strike of vertical beds & 2< i Basalt 52 <<«€ <<<<. Trace of Ste hed “wig-fa Inclined working the surface 7 38 h . fils Chevrons point downward = p® 29-1008 329-1097 ~ a a Lamprophyre Mine shaft p Shaft going above and below levels A Head of winze } TRIASSIC Argillite and hornfels meres Quartz vein ¢ Foot of raise or winze Approximate outline of stope Contact, showing dip Stopes are filled in part Dashed where approximately 7 witty located or inferred tne N H ane Dump % Fault or shear zone, showing dip 229-1089 Dashed where approximately located Net or inferred Locality sampled and number so m- p Vertical fault Opencut y Strike and dip of beds 50 0 100 Feet After Roberts (1943, pI. 3) c ool 1 Later workings (dashed lines) Datum is mean sea level by E. N. Cameron, August 1949 FIGURE 14.-Geologic map of the Rose Creek mine workings, Pershing County, Nev. diopside, actinolite, feldspar, quartz, calcite, epidote, and zoisite in varying proportions. Minor amounts of . other minerals, including sulfides, are present in quartz veins or disseminated through the tactite. Pyrite and chalcopyrite are the common sulfides. The absence of garnet and prominence of pyroxene and amphibole dis- tinguish this deposit from the ordinary tungsten-bear- ing tactite of the region. Sampling was done mainly in the underground work- ings, because surface exposures are poor. One sample each of silicated marble and granite was obtained from surface outcrops. Sampling data are given in table 33; locations of samples are shown on figures 13 and 14. Analytical results of the sampling show that parts of the tactite bed contain beryllium in abnormal amounts, but that its distribution in the tactite is quite LOCALITIES IN NEVADA 81 irregular. For the six tactite samples analyzed the range in BeQ content is from 0.0032 percent to 0.024 percent, the average being about 0.007 percent. The average BeQO content of the rocks may, of course, differ markedly from this in view of the small number of samples taken. The beryllium-bearing mineral is not known. Tasum 33.-Beryllia in samples from the Rose Creek mine BeO Sample Description (urgent) 329-1095 Chip sample across full width of tactite (21-32 in.), northeast wall of winze, 80-85 ft above bottom________.______ Chip sample across full width of tactite (16-29 in.), intersection of sublevel and Winze ... . 2. o .on e uals ld l oe a malneta nie an Chip sample of 3-ft thickness of quartzite overlying tactite at locality of 329- 1097. -: Je nen oie ~ cannt Chip sample across full width of tactite (15 in.) at east end of sublevel_______. Chip sample across full width of tactite £113 in.), junction of upper adit and raise 1 1097 . 024 1098 . 0015 . 0074 1099 1100 0: 1 .X: ae ec . 0042 Chip sample across full width of tactite (13 in.), underhand stope, upper adit level, 25 ft southwest of raise No. 2... Chip sample across full width of tactite (2.5 ft), east end of stope extending down from upper adit level, 45 ft inside portal. c_. .cc. L geal aige ben Chip sample of 5-ft thickness of gray hornfels, footwall of tactite, portal of upper adit... cnn Chip sample of black hornfels overlying tactite, opencut at portal of upper 1101 . 0047 1102 . 0082 1103 . 0013 1104 adit. _. l mca Jil} <. 0001 Chip sample of silicated marble from ridge southeast of tungsten Chip sample from granite outcrops south- east of tungsten mine.. _......_____. 1105 1106 . 0012 . 0015 Roberts (1943, p. 13) estimated the amount of ore in the mine to be about 6,000 tons but a large part of the ore between the sublevel and the surface appears to have been subsequently removed. It is doubtful that more than a few thousand tons of tactite remains in the mine. That much larger reserves might be dis- closed by further development seems unlikely. RAGGED TOP AREA The Ragged Top tungsten mine is on the west side of the Trinity Range, in sec. 11, T. 25 N., R. 28 E., Lovelock quadrangle. It is accessible from U. S. high- way 40 by about 8 miles of gravel road leading west from Toulon. The mine consists of a series of small shafts, opencuts, adits, and test pits excavated to ex- plore scheelite-bearing tactite deposits along the con- tacts of limestone and granodiorite. The mine is described briefly by Kerr (19462, p. 192) and was mapped during World War II by Ward C. 0. 0033 Smith of the U. S. Geological Survey. It is near the southeast edge of an area of granodiorite containing inclusions or pendants of limestone. The limestone patches are contact-metamorphosed, along their mar- gins where in places tactite containing scheelite is formed. Most of the tactite bodies are small but one about 1,000 feet northwest of the mine has a strike length of more than 1,000 feet (fig. 15). 'Since Smith's map was made, a series of shallow cuts and trenches has been excavated along the length of the tactite body. These excavations indicate that the body is more complex than was supposed. In trench A (fig. 15) it consists of two principal southeast- ward-dipping layers of garnet and garnet-diopside tactite separated by a limestone parting. The lower layer of tactite is probably about 15 feet thick, and the limestone parting probably has roughly the same thick- ness. The upper layer may be as much as 35 feet thick, but this figure includes a few feet of limestone. The lower layer is exposed in trench B, but its thickness of southeastward-dipping beds abutting against grano- diorite includes about 4 to 5 feet of tactite in two layers separated by 5 to 6 feet of limestone. The bot- tom of the lower layer is not exposed, but it probably is not more than a few feet thick. Trench C exposes a single zone of tactite, 18 to 25 feet wide, containing blocks of silicated marble. In cut E a width of 62 feet of tactite is exposed, but the mass appears to be dipping gently to the southeast and may bottom on granodiorite at shallow depth. At the head of the cut it contains a mass of blue limestone and silicated marble. North of this cut the width of tactite decreases and it finally pinches out, though small pods of tactite are present here and there along the granodiorite- marble contact for some distance. Samples taken from the tactite body are described in table 84. TaBu® 34.-Beryllia in samples from the Ragged Top area Sample Description R (pg-603!) 329-1182 Chip sample along 110 ft from upper tac- tite layer (which includes limestone parting) to east edge of trench A___._. <0. 0001 1183 Chip sample covering 8 ft along western end of trench A, from upper part of lower tactite . 0016 1184 Chip sample, full width of lower tactite Jayer, trench B..:.c.li-_geeducuy lew. . 0014 - 1185 Chip sample of silicated marble forming parting 4.5 ft thick between tactite layers trench . 0005 1186 Chip sample across full width of tactite jayer, cut B. . uuu. . 0016 1187 - Grab sample of granodiorite from chunks of rock on dump of Ragged Top mine. . 0013 1188 Chip sample of tactite from low knoll east of mine road 2,300 ft N. 10° E. of north end of tactite body shown on figure 15. . 0019 82 OCCURRENCE OF NONPEGMATITE PPA Tak / _ ./ Afpf> TRENCH D Az TRENCH _C ~>4 Te. pie ‘ 6/2791] al ¢ I d \ TRENCH R !.; a a" s * A ( & 4 {ts * | \ I \ e mck '% BERYLLIUM IN THE UNITED STATES 4 C C 98 /\N\\\ Tor sizt-6ze Kw\\\ Aff P\ ST // @ 349505 13 TSATA A TOH 1.3 zz \/ % s104 A10f8 30 HLYON 3041 1 Epos 13 88 LOCALITIES IN CALIFORNIA 89 below the level, which is at altitude 4,997. The lower adit connects with these workings at a point southwest of the incline. The beds are much faulted and are dif- ficult to trace in some parts of the mine. 'The middle adit level (glory hole level) and the level developed from the inclined shaft, which are the most important of the western workings, are shown on figure 17. The eastern workings consist of three adits and ap- pended underground workings that expose a third tac- tite bed. This bed dips westward and is stratigraph- ically below the tactite beds in the western workings. The two upper adits are short; the lower and main adit is about 175 feet long and leads to drifts, a winze, and several raises (see fig. 18). The rocks explored by the workings are a varied as- semblage of blue limestone, white to gray marble and silicated marble, cale-silicate rock, calc-hornfels, and tactite. The general geology of the mine area is shown in figure 19. The rocks are prevailingly thin-bedded and show marked changes in mineral composition across strike. The beds overlying the upper tactite layer, in order of stratigraphic sequence from top to bottom, are rib- bon tactite, consisting of alternating thin layers of garnet-rich and diopside-rich rock, gray to white mar- ble veined by silicates, calc-silicate rock interlayered with tactite, and idocrase-bearing marble. The prin- cipal beds of the upper tactite layer are garnet-rich tactite and garnet-diopside ribbon tactite. A spotted tactite bed of undetermined mineral composition is present in the glory hole. The rock underlying the upper tactite layer and separating it from the lower tactite is thin-bedded calcareous shale, largely altered to calc-hornfels. The lower tactite layer is similar in composition to the upper tactite. These rocks consti- tute a more varied assemblage than those of most tactite TRUE NORTH EXPLANATION . ads E1. 5190 ft \ I 7 7 7 : . 7 ( Sf; ~ AAZq j; t ra trey 3 Granite Limestone 0 5p» \/‘/_ is 3 u Partly covered o At 2a \Andesite dike p t s a> & o AVR S & R If : E1 Scheelite-bearing tactite | 2 ss Tex & Shale and hornfels vip ~ venta tall... Contact, showing dip Dashed where approximately located; dotted where concealed Barren tactite ied Rhees Hate mice Fault, showing dip Dashed where approximately located or inferred (Fa tas 329-1289 and 1290 £70 ’\> yn i_ Strike and dip of beds ay \ a asso- s a ar $2. A 2-foot gouge and breccia zone along fauls 1/7/ IAF Head of winze \/\‘>/<\P£/ I /|\/ PEt > iS 28 (ed x.y / XX Foot of raise or winze x/y" y* ious Say" {~- inclined sy % zl, Localit 329-1287. _-. 60 222, ality sampled and number ©% 4 pz, . ¥ z Biotite schist and «go. tz, 329-1286 n y_320-1288 feldspathized T / a hornfels > tassa _J, ,, to 1285 ga §§§\ f'.’ = \n \ ® P ~ | 6-inch gouge zone along fault Hard greenish garnet rock After Lemmon, 1941, pi. 77 50 0 100 Feet 1 1 1 1 1 | _3 1 Datum is approximate sea leve/ FIGURE 18.-Geologic map of the lower eastern adit, Round Valley mine, Tungsten Hills, Inyo County, Calif. 467945-59 T 90 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES otta pupa, \\\\\\\\\\\ <8 _" § P hi 3 y " 2-2 W -Zm® ”I: 44 /, 1///I ll} so 329-1278 Alluvium Marble Hornfels and schist Tactite and light-colored calc-hornfels, _- contains little or no scheelite Tactite with scheelite \\\\ I \\\\\\\\\ seo & / 1530 Feet 3 dala". 1 N € Contour interval 10 feet atum is mean sea level EXPLANATION lll, Contact __ atty Dashed where approximately ( Dump located or inferred 3 48 329-1278 mare mew o f Fault, showing dip Locality sampled and number 5 Dashed where approximately located or inferred 90 --- Vertical fault Building "150 Strike and dip of beds Rim of glory hole or opencut a Mine shaft After unpublished map by P. C. Bateman | and M. P. Erickson FIGURE 19.-Geologic map of the Round Valley mine, Inyo County, Calif. LOCALITIES IN CALIFORNIA 91 deposits and were, therefore, sampled in detail. The samples are described in table 41. TaBt® 41.-Beryllia in samples from the Round Valley mine BeO Sample Description (percent) WESTERN WORKINGS Beds overlying main tactite: Chip sample across lower 14 ft of inter- layered calc-silicate rock and tactite, Chip sample along three lines at 5-ft in- tervals across idocrase-bearing marble immediately above tactite, inclined- shaft level.. . eoue ls Chip sample across outcrop of ribbon tac- tite, 300 ft southwest of glory hole.... Chip sample across marble outcrop, 50 ft south of glory hole.__.._L_.__.__..___. Beds of main tactite zone: Chip sample at intervals across spotted fiagtite layer, southwest wall of glory igh aomk -n Chip sample across garnet-diopside tac- tite, southwest wall of glory Chip sample across garnet diopside ribbon tactite, north side of glory Chip sample across garnet tactite, inclined shaft level . 20%) o_ cleans aekn=- red ane Beds underlying main tactite: Chip sample of 744 ft of calc-hornfels, east side of glory hole at adit Chip sample of 744 ft of calc-hornfels im- Ilrétzgiately below beds of sample 329- 329-1271 (27s <0. 0001 . 0024 <. 0001 <. 0001 4278 1279 329-1269 . 0045 <. 0001 <. 0001 . 0019 / 1270 1272 1276 329-1267 1268 . 0006 . 0003 1280 Chip sample of 10-ft thickness of calc- hornfels from shallow cut at northeast edge of glory hole......:.....:....... Lower tactite zone: Chip sample across '7-ft thickness of banded garnet-diopside tactite, glory- hole } c cen " calc.. <. 0001 Chip sample of 15-ft thickness of cale- silicate rock containing coarse patches of light-pink garnet, glory-hole level___ Grab sample of garnet-tactite from dump fif lsmall glory hole east of main glory OC... sam ss . 0017 329-1273 1274 . 0018 1281 . 0017 LOWER EASTERN ADIT 329-1282 Chip sample across 55 in. of fine-grained garnet tactite containing a few thin layers of cale-silicate rock___________. <. 0001 Chip sample of thinly laminated light cale-silicate rock, 25 in. thick________. <. 0001 Chip sample across 37 in. of thinly lami- nated limestone, poorly silicated_____. <. 0001 Chip sample across 41 in. of thin, alter- nating tactite and cale-silicate rock.. <. 0001 Chip sample across entire thickness of shale <. 0001 <. 0002 . 0001 1283 1284 1285 1286 1287 1288 1289 and hornfels;...s2. .-... tne Chip sample across 5-ft thickness of bio- tite schist (feldspathized Chip sample of granite, 1 to 5 ft from fault contact with limestone..____________. ___ Chip sample of granite showing full tex- tural range from aplite to fine-grained peginatite. L . case inasss Chip sample of vaguely defined dike of aplite; 2 /ft wide.... _.. __. .l I . 0007 . OO11 1290 RESULTS OF SAMPLING As in adjacent districts, the results of the sampling show that beryllium occurs somewhat more abundantly in tactite than in other rocks. In general however, the beryllium content of tactite deposits in the Tungsten Hills is low and compares to that of tactite deposits in the Mill City district, Nevada. The production of tungsten in both districts has been large and, inasmuch as tungsten and beryllium tend to be associated in tactite deposits, the scarcity of beryllium is puzzling. At the Round Valley mine the presence of idocrase and the occurrence of ribbon tactite that is structurally, though not mineralogically, similar to that at Iron Mountain, N. Mex., might be taken as indicators of helvite, but none was found. Only two samples from the Tungsten Hills-329-1255 from the Little Sister mine and 329-1269 from the Round Valley mine-con- tained more than 0.0025 percent BeOQ. These samples contained 0.0036 and 0.0045 percent BeQ, respectively, and reserves of these grades probably are small. Be- cause of the large number of samples taken at the two mines, there seems small hope that larger deposits of better grade would be revealed by further sampling. Though sampling at the Aeroplane mine was less exten- sive, the fact that beryllium was not detected in any of the samples collected is discouraging. PINE CREEK DISTRICT PINE CREEK TUNGSTEN MINE The Pine Creek tungsten mine is in the northern part of the Mount Goddard quadrangle, 1 mile southeast of Mount Morgan, in the Sierra Nevada. The mine is reached from Bishop, Calif., by way of U. S8. Highway 395 to Round Valley and thence by paved and gravel roads. The history of the mine and discussions of the tungsten-molybdenum-copper ore bodies have been given by Lemmon (1941b, p. 89-91) and by Bateman (1945). The deposits have been worked intermittently since 1916. Operations since 1938 have been conducted by U. S. Vanadium Corporation. A visit to the mine was made with Bateman on August 26, 1949. The ore bodies are in a contact zone between marble and intrusive quartz diorite. The contact zone consists mainly of garnet-diopside tactite but includes quartz- epidote tactite, quartz, and quartz-feldspar rocks. Thicker parts of the contact zone constitute the ore bodies. The ore minerals are scheelite and molybdenite, with minor amounts of chalcopyrite and bornite. Gangue minerals are quartz, garnet, diopside, epidote, and feldspar. Five ore bodies crop out in the area of the Pine Creek mine. All contain tungsten in com- mercial amounts but only the North and South ore bodies contain molybdenum in important quantities. The geology in the vicinity of these two ore bodies is shown in figure 20. 92 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED Samples 329-1260 to 329-1263 +/+ North ore body +o 4 + Samples 329-1258 and Contact r-- 329-1260 Locality sampled and number 0 200 Feet After Bateman, 1945, pl. 37 Wd FicurE 20.-Geologic map of part of Pine Creek mine area, Inyo County, Calif. The South ore body is in a prong of altered marble that extends into the quartz diorite.' In the opencut the ore body is 300 feet long and 150 feet wide; its width diminishes with depth. The ore dips steeply east and rakes 60° S. Near the center of the body are two horses of cale-silicate rock and silicated marble. The North ore body is largely covered. Sampling data for the Pine Creek mine are given in table 42; locations of samples are shown on figure 20. TaBu® 42.-Beryllia in samples from the Pine Creek mine BeO Sample Description (percent) 329-1258 Chip sample across silicated marble, 35 ft AMok IE Cred eee bere ae aap aan ae 0. 0016 1259 Chip sample across tactite beds, 12 ft thigk s. 0 seee nu a ber ak 4 e =o + a ul mid . 0018 1260 Chip sample across 10 ft of silicated mar- ble adjoining the tactite____________. <. 0001 1261 Chip sample across tactite layer_______. . 0037 1262 Chip sample of quartz diorite next to tac- Se.. .. Janak edes anl an . 0044 1263 - Chip sample across 15-ft thickness of mar- ble forming east wall of ore body.____. . 0014 TAILINGS FROM MILL OF TUNGSTAR MINE The Tungstar mine is on the west shoulder of Mount Tom, at an altitude of 12,000 feet, in the northern part of the Mount Goddard quadrangle. The mine was worked for tungsten in the early 1940's, and the tactite ore was milled in Pine Creek Canyon below the mine. The mine is closed and the mill has been destroyed, but STATES the tailing dumps remain. Two samples were taken. Sample 329-1265, consisting of handfulls of material taken at intervals along the edge of the main and older pile of tailings, contained 0.0058 percent BeOQ. A simi- lar sample (329-1266) from the newer pile of tailings contained 0.0021 percent BeQO. YANEY TUNGSTEN PROSPECT, BISHOP DISTRICT The Yaney prospect is at the base of the Sierra Ne- vada, about 5 miles southwest of Bishop, Calif. Work- ings consist of an opencut leading to irregular stopes in the upper part of the deposit, and an adit, at a level about 50 feet lower, leading to drifts. A brief inspec- tion of the deposit was made with Paul C. Bateman, on August 29, 1949. Bateman furnished the information on which the following description is based. The workings are in an altered tactite deposit along the contact of metasedimentary rocks and granite. Ap- parently the deposit originally was an assemblage of tactite and silicated limestone beds similar to those exposed in the deposits of the Tungsten Hills to the west. Subsequently, parts of the deposit were altered to a mixture of friable opaline silica, ocher, and jaro- site, in various proportions. Alteration has been in- tense in places, and large masses of the alteration prod- ucts are present. Some of the altered material contains crystals of ferberite 4; to 4 inch in diameter which are apparently pseudomorphs after scheelite. The average grade of the ore is about 1 percent WO;. Unaltered tactite is exposed in the lower workings, but it is barren of scheelite. In places the tactite is altered to a clayey material. Samples taken at the prospect are described in table 43. TaABL® 43.-Beryllia in samples from the Yaney prospect BeO Sample Description (percent) 329-1295 White opaline material, entrance cut, upper <0. 0001 1296 Jarositic material with ferberite, entrance out, upper <. 0001 1297 Ocherous material, entrance cut, upper \ working - =". 22... Une recon Lu . <. 0001 1298 Ferberite-rich material, entrance cut, upper workings. .. <. 0001 1299 Clayey material, lower workings-___.._. <. 0001 1300 White opaline material, ferberite free, lower level_____._ (o anl ou aii ines a - - <. 0001 1301 Unaltered tactite, lower level__________._ <.. 0001 1302 Nearly unaltered cale-silicate rock, lower Jevels_ O 5 OOo Lol t oue pout _ <. 0001 SAN BERNARDINO AND KERN COUNTIES ATOLIA DISTRICT The Atolia mining district in southeastern California straddles the boundary between San Bernardino and Kern Counties. Paved roads connect the district with Randsburg and Johannesburg, 4 miles to the north, and with Kramer, 23 miles to the south. Tungsten was dis- covered in the area in 1904, and placer and lode mining LOCALITIES IN ARIZONA 93 have been carried on intermittently. In late August 1949 a few of the mines were being operated on a small scale by men working under leasing arrangements with the Surcease Mining Co. The district has been de- scribed by Hulin (1925) and Lemmon and Dorr (1940). Tungsten is found both in lode deposits and placer deposits. The lode deposits are veins that strike N. 75° E. to N. 75° W. and dip 45° N. to 85° S. Faulting during and after deposition of the minerals has compli- cated the structure of the deposits. The veins consist of scheelite in a gangue of quartz and carbonates, with pyrite, stibnite, and cinnabar. The scheelite ore bodies occur as steeply raking shoots as much as 1,260 feet in strike length and 1,080 feet in known pitch length. In places the ore is as much as 17 feet thick. The wallrock is quartz monzonite. The placer deposits are concen- trations in Quaternary alluvium that blankets the area of the tungsten vein. UNION MINE The Union mine, largest producer of the district, has been worked to a depth of more than 1,000 feet. It con- sists of a series of inclined shafts leading to 14 levels; the main shaft was the only one open at the time of inspection. The workings are drifts, raises, winzes, and inclined stopes in two veins, the North vein and the South vein. The veins strike east-northeast and dip 40°-63° N. In the western part of the mine the veins are as much as 180 feet apart; eastward and downward the veins converge, intersecting at a low angle in the eastern part of the mine. Each vein con- tains one principal shoot. In the most productive parts of the veins, the strike lengths of the shoots range from 600 feet to about 1,000 feet. Samples taken at the mine are described in table 44. TaBL® 44.-Beryllia in samples from the Union mine BeO (percent) Description Chip sample across full width of north vein; 9th level, 200 ft west of main shaft, small stope upward from level.. Chip sample across 18 in. of wallrock on either side of vein. Same locality as sample 1907... l- ecus Chip sample across full width of branch vein extending from south vein into hanging wall; 9th level, crosscut about 80 ft east of main shaft.___ _. ____.__._ Chip sample across full width of south vein zone (8 ft wide) consisting of shattered quarts monzonite cemented by quartz, carbonates, and scheelite; sublevel between Oth and 10th levels, 200 ft cast of shaft...-.«............ Chip sample across full width of mineral- ized zone, south vein; stope 100 ft east of main shaft, 40 ft below 9th level.__. Chip sample across horse of quartz mon- zonite separating two parts of south vein. - Same locality as sample 1311... Sample 320-1307 <0. 0001 1308 <. 0001 1309 <. 0001 1310 <. 0001 1311 <. 0001 1312 <. 0001 FLATIRON-SPANISH VEIN SYSTEM The Flatiron-Spanish vein system is an easterly- trending Y-shaped system of steep northeast-dipping linked veins. The stem of the Y is to the west. The Flatiron vein system forms the stem and south branch of the y; the Spanish vein forms the north branch. The deposits are in general similar to those of the Union mine. Two samples were taken in the vicinity of the inter- section of the two vein systems. Sample 3829-1314 is a grab sample of ore from a stringer two to four inches thick in a small stope. Sample 329-1315 is a grab sample of pieces of high-grade ore from the ore piles. The samples did not contain as much as 0.0001 per- cent BeO. ARIZONA By Wiruram: T. Houser Field investigations for beryllium in nonpegmatite rocks in Arizona were undertaken in August 1949 by W. T. Holser, assisted by W. I. Finch. The districts from which samples were taken are shown on figure 21. Traces of beryllium had been found previously in samples from the pyrometasomatic deposits at the Christmas, Clifton-Morenci, and Old Hat districts; no additional work was done in these areas. The most promising resources of nonpegmatite beryllium in Arizona are in beryl-bearing tungsten veins at Boulder Creek, Yavapai County ; the Tungsten King mine, Little Dragoon Mountains, Cochise County; and the Boriana mine, Mohave County. Pre- vious sampling in the San Francisco district, Mohave County, in connection with the Mine, Mill, and Smelter Survey, indicated the presence of beryllium in epi- thermal gold-silver veins. The only pyrometasomatic deposits in which beryllium was found are in the Dra- goon Mountains, Cochise County. COCHISE COUNTY DRAGOON MOUNTAINS The Dragoon Mountains rise steeply from the desert 12 miles northeast of Tombstone, to an altitude of more than 7,500 feet (fig. 22). They have a northwesterly trend from the old mining camps of Courtland and Gleason for about 22 miles to Dragoon, a station on the Southern Pacific Railroad. A graded dirt road from Tombstone provides access to the southwestern side of the range, from where the mines are reached by steep mountain roads. The geology of the Dragoon Mountains has been de- scribed by Darton (1925, p. 292-296) and by Gilluly (1941). Precambrian Pinal schist is overlain by Bolsa 94 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 369 7 +R / V ER 34° 2% 114° 112° 110° F A six =.= EXPLANATION / \ oA I .@ Locality sampled for this report e mL *> x 11 \ Other sampling Ld | I I Flagstaff "\\.J 1 o | 1-36 - % 1 | f % > 1 / i 32 \ / ( A m ~ m 09 bo h 114° Cochise County . Courtland-Gleeson . Gordon and Abril mines . Little Dragoon Mountains . Tombstone 112° J O -O Mohave County 5. Boriana __ 6. San Francisco Pima County . Empire . Helvetia . Pima ©o0=1 1?i0 Miles Santa Cruz County 10. Patagonia Yavapai Coufity 11. Boulder Creek FigUrE 21.-Index map of localities sampled in Arizona. LOCALITIES IN ARIZONA EXPLANATION 329-549; 0.004 Sample number ; percent beryllia R /‘ OLDEN RULE MINE L-5000 eC 32° 007 Pearce z CGORDOoN MINE 0.007 3 Y A 0.04 329-547; 329-543; ~d TRUE NORTH 1 0 1. vse 1 Is. 1 1 Contour interval 500 feet Datum is mean sea level 1 10700’ Base from U. S. Geological Survey Dragoon, Cochise, Benson, and Pearce quadrangles 109°50' " FicurE 22.-Index map of beryllium occurrences in Dragoon Mountains, Cochise County, Ariz. | 96 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES quartzite and Abrigo limestone of Cambrian age. Con- formable on the Abrigo limestone are 350 feet of mixed shales and limestones of the Martin limestone of De- vonian age which are succeeded by at least 700 feet of massive Escabrosa limestone of Mississippian age. A thick section of limestone of the Naco group of Penn- sylvanian and Permian age overlies the Escabrosa lime- stone. The rocks of Paleozoic age have been de- formed and invaded by intrusive rocks of Cenozoic age, chiefly the Stronghold granite. After erosion the re- gion was covered by sandstones of the Upper Creta- ceous and Tertiary volcanic rocks. The geology has been complicated further by thrust faulting. Metamorphism of the sedimentary rocks of Paleozoic age has been particularly intense near their contact with the Stronghold granite. The Escabrosa limestone and part of the Naco group are changed to white marble with some tremolite. The more argillaceous parts of the Martin and Abrigo formations and the Naco group contain large quantities of andradite, hedenbergite, and epidote. Garnet also occurs in the sedimentary rocks along a fracture zone several thousand feet from the granite, and some metamorphism is found as much as 5 miles from the granite outcrop. There has been little mining activity other than in the Courtland-Gleason district at the south end of the range. A small production has been credited to the Dragoon and Johnson (Cochise) districts. The Golden Rule mine, producing principally lead, at the north end of the range and the Middlemarch mine, producing principally copper, on the eastern side, were the only producers before World War II. The Gordon mine, on the southwest crest of the range, reportedly pro- duced lead-zinc ore during World War II. The Abril mine, on the western slope, has been the source of con- siderable zinc since 1945. All of these mines are in sedi- mentary rocks close to the border of the Stronghold granite. The dominant ore minerals at the Golden Rule, Gordon, and Abril mines are chalcopyrite, galena, and sphalerite; the gangue minerals are garnet, epidote and specularite. Samples from the Dragoon Mountains contain as much as 0.04 percent BeO (fig. 22). Although the beryllium-bearing mineral has not been identified, the analogy to other beryllium deposits suggests that hel- vite may be the source of the beryllium. The similarity between the ratios of beryllium and base metals in ore and gangue indicate that the beryllium is associated mainly with the ore. The amount of beryllium in the tactite at the Gordon and Abril mines is at least 10 times that found in 85 percent of the tactite deposits sampled in the Western United States. COURTLAND-GLEESON DISTRICT The Courtland-Gleeson district (Turquoise district) is in the southeastern part of the Dragoon Mountains, 15 miles east of Tombstone. The geology of the dis- trict was described by Ransome (1913) and by Wilson (1927). Limestones of Paleozoic age and shales and sandstones of Cretaceous age have been intruded by a variety of igneous rocks of which quartz monzonite porphyry is the most widespread. Contact metamor- phism of the sedimentary rocks near the intrusive por- phyry has been slight. Locally minor quantities of garnet, epidote, quartz, and pyrite have formed in the Abrigo limestone of Cambrian age. At least three periods of normal faulting and one of thrust faulting have been recognized. Deposits containing disseminated chalcopyrite and minor quantities of galena occur in the metamorphosed Abrigo limestone. Oxidized copper minerals are com- mon in the upper parts of the deposits. According to Ransome (1913, p. 533), the copper mineralization was simultaneous with the silication. The Humbot mine (Wilson, 1927, p. 55-56) is typical of these deposits. A 22-foot channel sample (829-551) was cut through garnet-epidote tactite from an outcrop 30 feet west of the Humbot shaft. A composite grab sample (829- 552) of chalcopyrite-pyrite-specularite ore with garnet- epidote gangue was taken from the dumps of the Humbot and Highland mines. These samples did not contain as much as 0.0001 percent BeQ. GORDON MINE The Gordon mine is near the southwestern crest of the range at an altitude of 7,000 feet, about 14 miles by graded dirt road from Tombstone. The mine work- ings include three adits. The principal ore mineral is galena. It occurs along a west-trending fracture zone in the Abrigo limestone, a few hundred yards east of a mass of Stronghold granite. On the surface the fracture zone is 50 to 100 feet wide and can be traced for half a mile along the strike. In and adjoining the zone of fracturing are interlayered thin-bedded cherty limestones and epidote- garnet-specularite tactite. A T-foot channel sample (329-547) taken across the tactite at the portal of the northern upper adit contained 0.007 percent BeQ. According to Mr. J. H. Macia, the mill at Tombstone was built during World War II to treat the ore from this mine. A grab sample (829-543) of ore from the receiving bin at this mill contained 0.04 percent BeO and 0.0X percent each of bismuth and cadmium. LOCALITIES IN ARIZONA 97 ABRIL MINE The Abril mine is at an altitude of 7,000 feet on the steep western slope of the Dragoon Mountains. The mine is accessible by a dirt road that leads from the southwestern side of the range. The mine was de- veloped by Bargain Mines, Inc., in 1945. From 1945 to 1948 it was operated by the Shattuck-Denn Mining Corp., and about 20,000 tons of lead-zinc-copper ore was processed in their flotation mill at Bisbee, Ariz. The ore was carried on an inclined tramway to the bottom of Stronghold Canyon, whence it was trucked out. The mine workings consist of several adits driven in a large block of Escabrosa(?) limestone, that is nearly surrounded by Stronghold granite. The lime- stone and interbedded shales have been metamorphosed to hornfels, marble, and tactite. Sphalerite and chal- copyrite fill small fractures and partly replace the epi- dote-specularite tactite. Some ore is found in garnet- epidote tactite. Samples of tactite (329-549) and of ore (329-550) from the dumps at the mine contained 0.004 and 0.02 percent BeQO, respectively. Specimens of ore from this mine contained 0.0X percent tungsten. LITTLE DRAGOON MOUNTAINS The Little Dragoon Mountains are in northwestern Cochise County. The principal settlement is at the old mining camp of Johnson, on the eastern side of the mountains. Copper and zinc ore are produced from the Republic and other mines. The Pinal schist of Precambrian age underlies much of the western part of the Little Dragoon Mountains. The schist is overlain by the Apache group of Precam- brian age, which includes conglomerate, shale, and sandstone. Sedimentary rocks of Paleozoic age, pre- dominantly limestone, are nearly conformable with the Apache group and are at least 2,500 feet thick. They constitute the Abrigo (Cambrian), Martin (Devonian), and Escabrosa (Mississippian) formations, and the Naco group (Pennsylvanian). Blocks of sandstones from the Bisbee group of Cretaceous age are faulted against the sedimentary rocks of Paleozoic age. Fol- lowing regional folding and faulting a body of quartz monzonite was intruded, cutting rocks as young as the Bisbee group. Dikes of aplite and lamprophyre cut the quartz monzonite and the country rocks. Sampling data for the little Dragoon Mountains are given in table 45 and the localities sampled are shown on figures 23 and 24. J. R. Cooper of the U. S. Geo- logical Survey, who had previously sampled some of the localities, conducted the party over the area and assisted in the sampling. Mr. Oscar Jarrell of the Coronado Copper and Zinc Co., «owner and operator 467945-59--8 of the Republic mine, generously furnished mill samples and analytical data. Mr. Edwin Over of Colo- rado Springs, Colo., supplied details concerning the occurrence of beryl at the Bluebird mine. Taser 45.-Beryllio and tungsten in samples from the Little Dragoon Mountains Percent ~ BeO? ws Sample ! Locality and description TUNGSTEN KING MINE 3290-435 436 437 Channel sample across 2.5-ft veins.. _____ o...... etl la te. Channel sample across 3 ft of chlorite schist between quartz vein and quartz monzonite_. Channel sample across 2 ft of chlorite schist with some 22-2 sons ae nem ninae a - ard Channel sample across 3 ft of altered quartz monzonite rock near sample 441..._......__. Chip sample of fresh quartz mon- 0. 0008 0. 0860 . 052 . 1340 . 010 . 0700 441 . 016 . 1340 442 . 0018 . 0014 . 0028 . 0016 444 BLUEBIRD MINE 329-446 Chip sample of 4-in. tungsten- bearing quartz-fluorite vein in quarts monsonite..__._._... Channel sample across 3.5 ft of quartz veins (1/3) and grei- senized - quartz - monzonite (AB) e cane ous oh a mele Specimen of fresh quartz mon- s 2 ah ls an is s a as 2 Specimen of greisen next to quarts vein: 3 Specimen of quartz monzonite with argillic alteration, 15 ft from vein at sample 2-_-___. <. 001 (4) 4 Specimen of quartz vein contain- ing huebnerite_._.:_L __... _. <. 001 (€) . 0005 _ . 0014 447 . 0019 _. 0034 . 0016 _ @ . 0028 __ JRC-1 JOHNSON CAMP AREA 320-449 Two-week composite of mill heads at Republic mine, June 1949. From 1200, 1500, and 1600 levels west. - Garnet-di- opside tactite, with some chal- copyrite and a Same as sample 449, but taken in May 1948, from higher .L .--. a a Same as sample 450, but tailings. 5. Channel sample across 18-in vein of quartz, with fluorite and sulfides, cutting across Abrigo limestone, Mammoth mine... _ 5 Idocrase separated from marble of the Naco group, Black Prince Grab sample of idocrase-wollas- tonite tactite, with copper sul- fides, from dump of Black Prince Specimen of garnet tactite, with chalcopyrite, sphalerite, and chlorite, from main ore zone in hgammoth ming-......:_s <. 001 (4) <. O01 (4) . 0007 8. OX 450 0007 ®. OX 451 0007 ®.. OX 453 . 0007 *. OX 454A . 005 $ 455 6 . O01 A JRC-5 C _____ Oe ece c eager i Specimen of epidote-tactite con- taining sulfide ore minerals, diopside, chlorite, garnet, and potash feldspar, from main ore zone, Republic mine_.___._... See footnotes at end of table, <. O01 (4) 98 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Tapur 45.-Beryllio and tungsten in samples from the Little Dragoon Mountains-Continued Percent Sample ! Locality and description BeO ? ws JOHNSON CAMP AREA-Continued 8 Bpecimen of diopside-tremolite tactite, with quartz and cal- cite, from Abrigo limestone above ore zone, Mammoth 9 Specimen of wollastonite-garnet- idocrase tactite from Abrigo limestone below main ore zone, Standard prospect.... 10 Specimen of idocrase-garnet- wollastonite tactite, with ore minerals in limestone of the Naco group, dump of Black Prince mine.......3.;..._.. <0. 001 () <. O01 (®) . 0023 (€) ! Samples bearing 320-numbers collected by W. T. Holser and W. I. Finch; those bearing JRC-numbers, collected by J. R. Cooper. ? Quantitative spectrographic determination by Saratoga Laboratories, unless otherwise noted. Ht Betetmination by Frederick Ward, U. S. Geological Survey, unless otherwise noted. 4 Not determined. 5 Spectrographic amalyses by J. D. Fletcher. BeO figures determined on plates exPosed for general scanning but not for precise determination of BeO alone. Semiquantitative spectrographic analysis by J. D. Fletcher. These samples also antaémfid 9509X percent Mo, but no extraordinary amounts of 24 other elements ee table 15. TUNGSTEN KING MINE The Tungsten King group of 12 unpatented claims is at an altitude of 5,200 feet near the head of Clark Can- yon on the western slope of the Little Dragoon Moun- tains. The mouth of this canyon may be reached by about 16 miles of unimproved road leading up Tres Ala- mos Wash from Benson, Ariz. According to Wilson (1941, p. 43), scheelite was discovered here in 1916, and during World War I the mine was developed by open- cuts and short adits. Mining was renewed during World War II but the production was small. The Tungsten King claims are along the northerly trending fault contact between quartz monzonite on the west and Pinal schist on the east (fig. 24). A quartz vein mined for scheelite follows the fault contact for most of its exposed length. The principal opening is a 275-foot adit which crosscuts the vein about 100 feet below the outcrop. The adit was partly flooded at the time of our visit, and we did not enter it. Drifts fol- low the vein for about 200 feet south and north of the adit. Many pits have been dug along the vein, partic- ularly north of the adit. Near the adit, the vein is as much as 6 feet thick and dips about 60° E., but north- ward the dip becomes less. The vein is composed mainly of fine- to coarse-grained quartz and contains also minor quantities of scheelite, beryl, feldspar (some altered to clay minerals) , chlorite, and muscovite. The wallrocks at many places along the vein have been silicified. The structure of the vein is complex, particularly along the hanging-wall side, where the quartz occurs as a discontinuous lens and as irregular veins that cut the schist. As shown in figure 24, the vein is offset in three places by steep cross faults. Near the top of the peaks east of the Tungsten King mine one of these faults cuts the small outlier of sedimentary rocks of Paleozoic age that overlie the schist. The displacements of the sedi- mentary rocks and of the vein indicate that the south side of the fault was moved downward about 2,000 feet. Beryl occurs in the vein as prisms 2 or 3 centimeters long and 2 millimeters in diameter, terminated by the pinacoid. It is readily distinguished from the sur- rounding milky quartz by a characteristic pale-blue (5B7/4) color (Goddard and others, 1948). Most of it is reticulated through the quartz, in radiating or par- allel groups. The beryl appears to be more common near the schist wall or near schist inclusions. Some was found in feldspar-rich selvage along the hanging- wall side of the vein. In the schist the beryl apparently is most abundant in small blebs and stringers of quartz or aplitic material that are common near the hanging wall. The beryl is very irregularly distributed and the quantity that may be readily seen is small. Scheelite occurs in small shapeless patches, sparsely and irregularly distributed through the quartz and to an even lesser extent through the schist near the vein. It fluoresces white, indicating the presence of some molybdenum. In a pit north of the adit (near sample 329-341 in fig. 24) wulfenite was found on fracture sur- faces and in small vugs. According to Wilson (1941, p. 43), chalcopyrite and galena are also found in the vein. We saw small cubes of limonite, pseudomorphous after pyrite, in the vein outcrop. Along the footwall of the vein the quartz monzonite is intensely altered and silicified. It has a platy struc- ture with some slicken-sides, as if it had been strongly sheared. The feldspar is altered to a clay mineral. Where the rock is apparently unaltered, as at the portal of the adit, it is similar to the quartz monzonite of Texas Canyon in the southeastern part of the mountains. Channel samples were taken from several exposures of the vein (fig. 24). Results of spectrographic analyses (table 45) indicate that locally the vein contains more than 0.05 percent BeQ. In general, however, the grade of beryl ore as determined by visual inspection in the vein is lower than indicated by analyses. Apparently, some beryl occurs in the chlorite schist adjacent to the vein. The continuity of the vein indicates a large re- serve of low-grade material, but the small size of the beryl erystals prohibit recovery except by milling. The beryl might be a valuable byproduct of a scheelite mill- ing operation. LOCALITIES IN ARIZONA "100 110° 05" fig un C e BLACK PRINCE __, JRG-10; 0.0023 PX 329-455; 0.001 f\’\_ \ 2" 2a, Ssg) n Ofl __ JRG-5, 6, 8; < 0.001 Johnson Camp 0 453: 0~~ 329-453; 0.0007 REPUBLIC JRC-7; < 0.001 Q’QJ 329-449 to 14° 451 0.0007 «Q x AY E| [(& 9 g 20 os "3 > i E § 2 ra g ===V 3 § zf/ € > \ 44/ P £ P IRC-2 to 4; < 0.001 §50-207, 9.0019 -z *p ass 0 0028 UEBIRD $ STANDARD 329-446; 0.0005 Base from U. S. Geological Survey Dragoon quadrangle, 1943 \ ¢. / JRC-1; 0.0016 JRC-9;<0.001 EXPLANATION Mine mentioned in text JRC-9;< 0.001 329-447; 0.0019 Sample number; percent beryllia 1 0 L i i i I 1 Contour interval 500 feet Datum is mean sea leve! 2 Miles d FiGur® 23.-Map showing localities sampled in the Little Dragoon Mountains, Cochise County, Ariz. BLUEBIRD MINE The principal workings at the Bluebird mine are in a group of 21 patented claims that are in the hills at the head of Texas Canyon. Several unimproved roads pro- vide limited access to the area (fig. 23). Tungsten was mined in this area as early as 1899 (Richards, 1904), and Wilson (1941, p. 42) reports that about 2 tons of huebernite per day were produced in 1940. The tungsten-bearing quartz veins of the Bluebird group are part of a vein system that trends northeast- ward from the head of Texas Canyon nearly to John- son. The wall rock is quartz monzonite, which has been intruded by aplitic and lamprophyric dikes. The main group of veins is in a zone about 600 feet wide. Rich- ards (1904, p. 264) describes the Bluebird vein as the best-defined one of this group. The space between walls is about 5 feet, but the ore is only 6 inches thick, Most veins in the area are only a few inches thick, and are bordered by a foot or more of greisen on either side. A small quantity of beryl was collected from one of the narrow veins by Mr. Edwin Over of Colorado Springs, Colo. The colorless beryl crystals were found with quartz and fluorite in a small opening at the local- ity marked "Beryl" in figure 23 (Boericke property). We saw no beryl during our sampling of this property. Analyses of samples from the Bluebird mine (see table 45 and fig. 23) indicate that the quartz veins are probably low in beryllium content. The greisen ap- pears to have only slightly more beryllium than the quartz monozonite. 100 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES mie ~ * a. fom A A * * 4 *! ¢ a # 4 » 1 # # s." *;" u t=" a820-443,0.0013- haunts & fin colo a TWL W \ tp he [C $ 7. 16 |, EXPLANATION #1, 9% A _‘\ > Ps is 5 B s Hoy / f. y cle ig 1" > 2 s o% < 3 Porphyritic quartz monzonite ,\\ n *)w e " y € 7\ Coull ce Quartz and limestone Tey ¥ 4-2) ( > S % al t > 4 1 yeas ao Pinal schist < N 7 a a is 4 i % f # rew Lear. al % ; s 7 Quartz vein, showing dip . Strike and dip of foliation 4 £ f st , " ag. Cf" fl, Contact Strike of vertical foliation t dines a C 72 t* g ® depts mim X 8 tute f Fault, showing dip Prospect pit n \\ Approximately located z 4 34 ws # t $e “\ fs 088) Vertical fault Adit rims? a _é5 329-436; 0.052 Strike and dip of beds _ Sample number; percent &..... & # beryllia 4 fat. / is u g = eme s Geology after G. A. Fair, 1981 590 0 1000 Feet FiGuUrE 24.-Geology of the Tungsten King claims, Cochise County, Ariz. LOCALITIES IN ARIZONA JOHNSON CAMP AREA The Johnson Camp area is on the east side of the Little Dragoon Mountains, about 2 miles northeast of the Bluebird mine (fig. 23). It is an old camp with ex- tensive workings from which has come a large produc- tion of copper and zinc ore. The Republic mine was active in 1949. The geology of the area has been de- scribed by Cooper (1950). The principal ore bodies in the Republic and Mam- moth mines are associated with fractures in a bed of contact-metamorphosed Abrigo limestone. The ore consists of varying proportions of chalcopyrite, sphale- rite, bornite, and pyrite, with a little molybdenite and scheelite, in a gangue of potash feldspar, garnet, epi- dote, diopside, quartz, and calcite. Analyses of speci- mens of typical ore and gangue that were collected by J. R. Cooper and of composite samples of mill heads and tails, that were furnished by the Coronado Copper and Zinc Co. indicate that beryllium is not abundant at these mines (table 45). The Black Prince and Peabody mines were developed on an outlying hill in the northern part of the area. The ore is partly in thin shaly layers of the Naco group and partly in lamprophyre. In addition to the usual garnet and quartz gangue, the ore is found also in ido- crase-wollastonite rock formed by metasomatism of limestone of the Naco group. Samples 329-455 and JCR-10 of the idocrase-wollastonite rock from the dump of the Black Prince adit contained 0.001 and 0.0023 percent BeQO, respectively. Along the outcrop . above the adit, green idocrase occurs in crystals as long as 3 centimeters in white, wollastonite-rich tactite. The idocrase crystals separated from this material con- tained 0.005 percent BeQ. The small amount of beryl- lium in the metamorphosed limestones of this part of the district apparently is contained in idocrase. Several quartz veins in the Johnson Camp area trend northwest. Sample 329-453 from a quartz vein in the Abrigo limestone above the Mammoth shaft contained 0.0007 percent BeQ. TOMBSTONE DISTRICT The Tombstone district, in western Cochise County on U. S. Highway 80, was visited on August 1 and 2, 1949. Mr. J. H. Macia of Tombstone kindly served as a guide to the mines and provided much information on their operations. The geology of the district was described by Butler, Wilson, and Rasor (1988). Sedimentary rocks of Paleozoic age nearly a mile in thickness, principally limestone of the Naco group of Pennsylvanian age, are overlain unconformably by more than 8,000 feet of ; sedimentary rocks of the Bisbee group of Cretaceous 101 age. After extensive folding and faulting, these rocks were intruded in the western part of the district by the Uncle Sam porphyry (quartz latite) and in the south- west by the Schiefflin granodiorite. Deposits of silver, lead, gold, copper, and manganese are associated with northeast-trending fissures and related structures. The principal ore minerals are galena, gold, chalcopyrite, and argentiferous tetrahedrite, or their oxidation prod- ucts. The wallrock at many of the mines is a sedimen- tary rock of the Bisbee group, but at some in the south- ern part of the district it is the more calcareous rocks of the Naco group. The limestone which is partially metamorphosed to garnet, epidote, and idocrase, crops out on Comstock Hill northwest of the town. Silicifi- cation of the limestone was irregular and apparently is related to dikes of the Schiefflin granodiorite. Three samples were taken in the Tombstone district. Sample 329-539 was of manganese ore from the dump of the Oregon mine, 1.5 miles south-southwest of Tombstone. Sample 329-540 was chipped from a 60- foot-wide outcrop of garnet-calcite marble just west of the Luck Sure mine, 1.2 miles south-southwest of Tomb- stone. Beryllium could not be found in either sample. A chip sample (329-546) taken along a 50-foot line across an outcrop of garnet tactite and tremolite-calceite marble near the top of Comstock Hill contained 0.0007 percent BeQO. MOHAVE COUNTY BORIANA DISTRICT Beryl-bearing quartz-tungsten veins occur at the Boriana mine in the Hualpai Mountains about 18 miles east of Yucca, a town on the Atchison, Topeka and Santa Fe Railroad. The mine has been an important producer of tungsten ore. The veins were not sampled, but descriptions by Hobbs (1944, p. 247-258) and Kerr (19462, p. 102-104) indicate that they may be potential sources of beryl. According to Darton (1925, p. 180), the Hualpai Mountains "consist of Precambrian granite and gneiss cut by dikes of porphyry and other intrusive rocks." The country rock of the veins is a roof pendant of phyllite in a large mass of biotite granite. The phyllite crops out over a belt half a mile wide that trends north- easterly. 'Its foliation is roughly parallel to the ver- tical instrusive contact. The phyllite near the contact is recrystallized to a fine-grained schist composed of chlorite and muscovite. The veins are parallel to the foliation of the schist, but are discontinuous, frayed, and have an echelon pattern. The principal gangue mineral is quartz which is accompanied by small quantities of fluorite, calcite, muscovite, and potash feldspar. Wolframite, scheelite, 102 chalcopyrite, and minor amounts of pyrite, arseno- pyrite, and molybdenite are the metallic minerals. Ac- cording to Hobbs (1944, p:; 254), "Some beryl was found in the veins on the 700-level and also in the veins which cut the granite at the surface." Veinlets of fluorite and muscovite cut the quartz in some places, and Kerr (1946a, p. 103) states that muscovite is most abundant near tungsten minerals. Scheelite replaces wolframite, and most of the sulfides were deposited with the scheelites. Some sulfides, with quartz and potash feldspar, are younger. Near the north end of the Boriana property, a sodic granite cuts across the phyllite. The veins decrease in width and increase in beryl content as they pass from the phyllite into the granite. The sodic granite is thought to be related to the source of the mineralizing solutions. Reserves of tungsten ore were estimated at 2,400 measured tons, 9,900 indicated tons, and 44,000 inferred tons (Hobbs, 1944, p. 258). There were about 150,000 tons of unmined vein material between the under- ground workings and the surface. The beryllium con- tent of this material is not known. The mine closed down in February 1943, and no additional production has been reported to date (1951). SAN FRANCISCO DISTRICT The San Francisco district is in the Black Mountains in southwestern Mohave County, near Oatman, a town on U. S. Highway 66. The southern part of the district is referred to as the Oatman district; the northern part as the Katherine or Union Pass district. Sampling by members of the Mine, Mill, and Smelter Survey during World War II indicated the presence of beryllium in the gold ores from this district. Although the district was not revisited during the present investigation, the results of the earlier sampling are of sufficient interest and importance to be included in this report. The geology of the district has been described by Ransome (1923), Lausen (1931), and Wilson, Cunning- ham, and Butler (1934, p. 80-115). Precambrian rocks are extensive in the northern part of the district, where a coarse gneissic granite intrudes schists and gneisses. The granite forms the wall rock of the veins at the Katherine mine. The most abundant rocks of the Black Mountains are a thick series of Tertiary lava flows. They range in composition from rhyolite to olivine basalt; andesite and latite are the most important wall rocks of the veins near Oatman. Quartz monzonite and granite porphyries intrude the flows. The lavas dip gently eastward, presumably as a result of movement of several hundred feet along steep normal faults. The principal mineral deposits are fissure fillings in parts of the fault zones. Although the volcanic wallrocks are OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES highly altered by both ascending and descending solu- tions, they have not in general been replaced by metals. Lausen (1931, p. 63-72), considers the veins to be epi- thermal and recognizes five stages in the deposition of the vein material. Most of the gold, with some silver in solid solution, was deposited with calcite, quartz, adularia, and fluorite during the fifth stage. Routine sampling in connection with the Mine, Mill, and Smelter Survey in 1948 revealed significant quanti- ties of beryllium in tailings of the Gold Road mill at Oatman and the Katherine mill at Katherine. Data for these and other samples taken from the district are listed in table 46.. Locations of the mines listed in the table are shown in figure 25. The sample containing oui th *ryro KATHERINE 3, \ ROADSIDE DAVIS Dam js J Mile bos a\ ~. © : a ct - 35° 10 ex \., C. a K > *ALL / size a ( 3 fae _ at. E ens i orem ,X“/ > o % sag ts" -is c MOSSBACK,, hz A e ele -~ blas, F ig o "ay h\<_ Led X . } 2 Ty. f GOLDROAD fm eel UNITED net EASTER RS LELAND 1 0 _ 1Mile ARA rom " | a ey ._ -- vivian REED J 43 BIG JIM BLACK EAGLE I2 w MITCHELL 35°00" g TOPOCK 28 MILES FIGURE 25.-Mines of the San Francisco district, Mohave County, Ariz. 0.03 percent BeQ, taken at the Katherine mill, is from a large deposit of tailings (about 150,000 tons), and no samples of the various ores treated in the mill are avail- able. The source of the beryllium in the sample was not determined. Tailings samples from the Chloride and other dis- tricts in the Cerbat Range did not contain as much as 0.001 percent beryllium. The deposits in these districts are gold-silver veins of more complex mineralogy (Schrader, 1917, p. 199-206; Thomas, 1949). LOCALITIES IN ARIZONA TaBug 46. -Beryllia in mill tailings from the San Francisco district [Analyst, John C. Rabbitt] BeO Sample Mill and location Contributing mines (percent) 85-MC-3 - Katherine; Roadside, 0. 03 Katherine. Arabian, Katherine, Frisco, Tyro. 9 _ Gold Road; Gold Gold Road...... . 006 Road. 5 - Tom Reed; Tom Reed, . O01 Oatman. Black Eagle, Ben Harrison. 10 - Louzon; Oatman .. Mossback-.__--.. <. O01 7 United Eastern United Eastern, <. O01 Mines Corp.; Big Jim. Oatman. 6 - Vivian Mining Co.; Leland, Vivian <. 001 Oatman. Mitchell. PIMA COUNTY EMPIRE DISTRICT The Empire district is in the Empire Mountains in eastern Pima County, south of U. S. Highway 80 and east of State Highway 83. A pyrometasomatic tung- sten deposit in the southern part of the district was sampled on July 31, 1949. The deposit is just east of the Hilton ranch house, on the road to State High- way 83. The deposit was mapped and described by Marvin.' Southeasterly-dipping limestone of the Naco group (Pennsylvanian) is intruded by quartz monzonite. Within 50 feet of the contact, masses of the limestone have been changed to tactite that contain garnet, diop- side, wollastonite, quartz, epidote, specularite, and some scheelite and copper minerals. Four samples (329-524 to 329-527 inclusive) were chipped from tactite outcrops between the road and the next canyon, which is about 900 feet northeasterly along the contact. Beryllium could not be detected spectro- graphically in any of the samples. HELVETIA DISTRICT The Helvetia district is near the summit of the north- ern end of the Santa Rita Mountains about 30 miles southeast of Tucson. The western part of the district around the old camp of Helvetia is reached by 14 miles of graded road leading east from U. S. Highway 89 at Sahuarita. The eastern part of the district is accessible by several unimproved roads leading west from State Highway 83. The geology of the district (fig. 26) was described by Schrader (1915, p. 91-140), Creasey and Quick (1943), and Johnson (1949). The principal sedimentary rocks are limestones of Carboniferous age and clastic rocks of Cretaceous age, both of which have been severely de- formed and cut by thrust faults. The eastern part of the district is intruded by quartz monzonite of Late ® Marvin, T. C., 1942, Geology of the Hilton Ranch area: Arizona Univ. M. Sc. thesis. 103 Cretaceous or post-Cretaceous age which has highly altered the country rock near its contact. The western part of the area is intruded by granite of probable Mesozoic age. The contact of the granite with overly- ing limestones in the western part of the area is along a thrust plane; the limestones contain bodies of tactite. The tactite, composed of garnet, quartz, diopside, actinolite, and wollastonite, forms the gangue for much of the ore. Creasey and Quick believe the metallic minerals, including pyrite, chalcopyrite, and minor amounts of scheelite, sphalerite, and molybdenite, to be later than the silicate minerals. Channel samples were taken of tactite, mainly in or near areas containing copper or molybdenum minerals. The general locations of the samples with respect to the geology is indicated in figure 26; descriptions and analytical results are given in table 4'. TABLE 47.-Beryllia in samples from the Helvetia district [Spectrographic analyses by J. D. Fletcher. BeO content determined on plates exposed for general scanning but not for precise determination of BeQ alone] Sample Description (prefignt) 329-510 Grab sample of hornfels and tactite, with chalcopyrite, from glory holes of Mo- hawk mine in Helvetia Wash, half a mile east of Helvetia____________--~.--.- Channel sample across 6 ft of garnet tactite, with pyrite, chalcopyrite, and molybdenite, from 40-ft sublevel of Leader Channel sample across 6 ft of diopside- garnet tactite, with chalcopyrite (in- cluding 1 ft of fault gouge with secondary copper minerals) from main level of the Leader mine 420 ft from portal____.___._ .. Channel sample across 20 ft of garnet tactite and marble overlying the granite, at portal of upper adit Heavyweight mine, 1 mile east of Chip sample from 25-ft outcrop of garnet tactite above King adit (Rosemont 1GASC): .. <2 aa Channel sample across 10 ft of garnet tactite, with quarts and copper car- bonates, from portal of adit on Rose- mont lease, 150 ft north of sample 516. . Grab sample of garnet-quartz-chalcopy- rite-pyrite ore from bin at King adit___ Grab sample of garnet tactite from dump of Narragansett mine.........._._.... Grab sample of garnet tactite, with chal- copyrite and pyrite, from dump of Daylight <0. 0004 512 . 0004 514 . 002 515 . 0004 516 <. 0004 517 <. 0004 <. 0004 <. 0004 520 521 523 . 0004 PIMA DISTRICT The Pima district is on the eastern slope of the Sierritas, about 25 miles southwest of Tucson. The district was visited on July 28 and 29, 1949. Thanks are due to Mr. G. J. Duff, Arizona manager of the Eagle-Picher Mining and Smelting Co., for samples from the San Xavier mine. The geology and ore deposits of the district were de- scribed by Ransome (1922, p. 407-428) and by Wilson (1950). Strata of Paleozoic age, mostly limestones, 104 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES P § aS o . I 1 i {£4 a a 5 B C. % i Egg 5 g v}: t € a f £ a in 2 € g 8 | v4 t 5 % $ 3 $8 "1 $f Sr 8 §; & O8. 5 # 2 & 25 o & i © + s bo% R S ® 6 & 58% 5 6 0 £ O g P1 "ss € 4 B ¥ ye $ Cl Tig $" ats i a $ €. S ab & g ¥ m 5 d w §§ T s & o 3 56 $ # 3 a a 3 § 5 § € § m & a hid = < 4 spode} ad AHVN ¢ r is - ~s31yN0 7311253, NYINH34 4,12de “£22th ”Wag snoagé) fore $9 fa An eA ille e eeu ; i 13409 -3M40 _ NVIMBWVD a a. t£o a € 2 = 6 $ 5 #E § & $ £ is 0 Ra $& % 6 in € 52 R 0 2% £*. s o 2 cov € vf § & 2 8a o 0 3 € F & 5 25 c 8 Es > ® § l E 5 Sr -= 69 2 & E f .5N 0 5 'L < 0 4 EVE —/l‘ -B 3 & 6 27° & at a 5 s "/te"le F m & & - #4 2 At E SWT 3 ('= |25 8 iz i F $6 5 oB a $ Lis- F £ < w B e < p is A 8 I+] O e a x a 3 F: mle. as o © 32 § 3 ~ 1 M 5 HLNON angi 6 S a A § id eA "1 g p , é it G E o 5A: C -g spss frae ¥ a g B //% T Pre & 35 8 fff $3 e s t Ill/M7500” y a 2.1. 13 p Z Z x a ~ 2 £ am el A a ¥ + TLT t ? & arr r T GZ Z Zr x v Z 2 HLT TO 2D, d l PV FET g & o 4 'th B az 0 & 0 0 & Aes: m (f sso 3% 5 spams "f a ce \§§§§§§§\\\\xxx\ . =% § & & \ 14: R S & \\ c ti. 9 =s a \ Ts? £ ad sto fe E C Ga \ el y4 Sut Rug Nm No \\\\\\\\ Sous o- > S ‘\ S S" 0°05 ; 1 1989 \a 3 A ya al 7% C. 7x" 8 \ "Al. on =S ®l e m ; 0 nr Y. ¢ 2a fel ts f aga ss & S74 a mar cf 22 8 1 \‘ << # 'cl o € 2 £, 4s pesos m w iC / f «o a wre #3 = %R z sa iff P og 5 23g) Ge? E- Sis B ©6| $-. a=! £*5 4 I 6] & ;o in 2 $ & 25) at. 10| + $ ao) 228 ~ AS ics 2 ® y SEs «G| §Ef § $ & box's & = 8 0 e LOCALITIES IN ARIZONA are intruded by coarse-grained rocks that range in com- position from quartz monzonite to granodiorite. Their structure has been complicated by extensive folding, thrusting, and block faulting. The ore deposits are pyrometasomatic in origin. The ore nearest to the con- tact of the intrusive rocks is in tactite that is predom- inantly andradite, with some quartz, epiodote, wollas- tonite, and hedenbergite. The metallic minerals, in- cluding pyrite, chalcopyrite, magnetite, and rarely scheelite and molybdenite, are erratically distributed along fissures. The San Xavier mine is in ore farther from the intrusive rocks, and the gangue contains less garnet and more hedenbergite; calcite-sphalerite-ga- lena-chalcopyrite ore replaces the gangue minerals along a fault zone. The localities sampled for beryllium are shown on figure 27, and the sampling data are given in table 48. TaBum 48.-Beryllia in samples from the Pima district [Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] Description (pigrecgnt) Channel sample across 8 ft of yellow gar- net tactite, with copper carbonates, at abandoned mine shaft.___......_..... 5.5-ft channel sample across quartz-limo- nite vein and garnet tactite, from pros- pect «3. Channel sample across 15 ft of garnet tac- tite, with copper carbonates, from workings east of abandoned shaft____. «+ Channel sample across 8 ft of garnet- hedenbergite tactite(?) from pit south of Minnic Grab sample of garnet tactite and copper ore from Copper Queen Channel sample across 15 ft of garnet tac- tite, with quartz veins, from outcrop 70 ft south of Copper Queen shaft_______ L. Chip sample across 150-ft outcrop of gar- net ._.... _ reno wasn Channel sample across 2.5 ft of garnet tactite in pit 60 ft southwest of Morgan MIME ert da- ccs - nan- te L.. 3-ft channel sample across quartz-scheel- ite vein, next to sample 501--_____--- <2 7-ft channel sample across quartz-scheel- ite vein in pit 250 ft southwest of Mor- gan mine. _... ._ _._. <. Chip sample across 45-ft outcrop of garnet tactite at shaft 600 ft north of Morgan =s alk Chip sample across 50-ft outcrop of garnet tactite 300 ft west of Morgan mine.___ _ <. Tailings, from concentrator at Sahuarita, Ariz. (garnet-calcite-galena sphalerite ore from San Xavier mine), April-July igen inane s < Heads from concentrator at Sahuarita, Ariz. average for July 1949 (ore from San Xavier Sample 329-490 <0. 0004 491 0004 494 0004 496 . O01 . O01 497 498 0004 0004 499 501 0004 0004 502 503 0004 506 . 0004 0004 507 508 0004 509 <. 0004 105 R3 E. me Rize. 00 see w A 00° 329-491,(0,0004 o \ meray, HILL $ ; . (0.0004 3. *. \ \ 329-1303 and 509, €0.0004 3 w (Samples from Sahuarita concentrator) olf L posh 3 Twin Buttes 329-497,0.001 29-498; (0.0004 a to 503; €0.0004 ; & EXPLANATION s. ©-329-496; 0.001 Locality sampled and number; percent beryilia {~- éifijfl/fig <2 [ 0 2 Miles Contour interval 100 feet Datum is mean sea leve! Ficur® 27.-Index map to locations of samples from the Pima district, Pima County, Ariz. SANTA CRUZ COUNTY PATAGONIA DISTRICT The Patagonia district is in southeastern Santa Cruz County, just north of the Mexican border. It is about 25 miles by graded road south of the town of Patagonia, Ariz., which is on State Highway 86. The district was visited on July 31, 1949. The geology of the district has been described by Schrader (1915, p. 292-348). The Washington-Du- quesne area, in which all the pyrometasomatic deposits are found, was mapped by Arthur Richards and A. L. Brokaw of the Geological Survey during World War II, and their unpublished report was used as a guide in the sampling. In this area a block of limestone of Paleozoic age is surrounded by intrusive bodies of quartz monzonite and granite porphyry. Masses of the limestone have been metamorphosed to garnet-quartz tactite, with minor amounts of hornblende, diopside, and wollastonite near the southern end of the block. The principal ore bodies consist of pyrite, chalcopyrite, bornite, and sphalerite along fractures in the tactite. 106 The following samples were taken : 820-528 25-ft channel sample from outcrop of garnet tactite, with minor amounts of quartz, chalcopyrite, and calcite, at collar of new shaft on California claim. Average sample of 20 tons of galena-chalcopyrite- sphalerite-pyrite shipping ore, from California claim. 4-ft core from the upper part of the tailings pond of the Duquesne mill. Chip sample from 50-ft outcrop of garnet-quartz tac- tite at road cut on Big Crop claim. Channel sample across 10 ft of hedenbergite-garnet- quartz tactite, with galena, sphalerite, chalcopyrite, and pyrite, from pillar of glory hole 300 ft S. 30° E. of Holland shaft. 6-ft channel sample from outcrop of garnet tactite, with limonite alteration, near Belmont shaft. Chip sample of garnet tactite, with iron and manga- nese oxides, from 50 ft of north end of large open pit on the south end of the Belmont claim. Channel sample across 25 ft of garnet-quartz tactite, with iron and manganese oxides, from prospect pit 200 ft east of sample 536. 538 6-ft channel sample of garnet tactite from adit on Empire claim. 529 531 532 533 535 536 537 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES tailings and probably represents the average of a large amount of ore from the district. Samples of concen- trates and tailings previously collected for the Mine, Mill, and Smelter Survey from the Nogales smelter, which was processing ores from the Patagonia district, also showed no more than 0.001 percent BeQ. YAVAPAIL COUNTY BOULDER CREEK AREA The Boulder Creek (Bagdad) area is in western Yavapai County, 25 miles by road northwest of Hill- side, a station on the Atchison, Topeka and Santa Fe Railroad. Two mines in the area have been active : the Bagdad mine at the town of Bagdad and the Hillside mine on Boulder Creek. Beryl occurs in quartz-tungs- ten veins at a prospect near the headwaters of Boulder Creek,. Although time did not permit a visit to the prospect during the present investigation, information concerning it was furnished by C. A. Anderson of the U. S. Geological Survey. The Bagdad region has been described by Anderson Speetrographic analyses showed no samples more | (1948, 19502 1950b), and the geology of the part > 9 9 than 0.001 percent BeQ. Sample 329-531 is a core of | drained by Boulder Creek is shown in figure 28. The 113° c Tov ilk! ¢ 'v. EXPLANATION 9 ,. Tis XY: $5 & a *has "'a oh > Z A a': ma AW a & q 7 01 0:1%%e €6 n \ /s Yy f Cett. Basalitic flows and -| E 3 PfR CD \/ conglomerate £o Z!} (NL. WOLFRAMITE - BERYL: y SSS - Banz a 185 n Sis Aal at NaN tN CKY A# f 4 S v Q 5 ‘_\\/\,\// te x’i',\"§b;'-4. 7 N "= P 25 1 Ay A \ _ Lat: 8 */ 2 a (/> -~ N e® \ ll A a ;/ Quartz monzonite E; N # o /‘\l/ ~ 9 ~ x* ". ~ <2 # 4] 1/1 1_,/\\ \i,\|/‘ pe pS v Vk E13, < -- U a Amare a ,> 3 4 4 \ Porphyntlgtblotlte z h ‘ALowlen; Peak : granite & y < x aA agora t. fj’jfff; E - |* Schist, quartz diorite, and gabbro > \/’\’\/\/\\1I_ i= f ¥ te Contact o Z z w T Mine or prospect / i- 7. G p rr 41114 $ § s ////;;;; \\':// it:» r p- 4 y 34°35/55;;//f/ »NXy vor MINE txt inn 6 dose z = = ns .E. "A ® 2 7 Ler rrr s Bagdad ;.: :.¢ 2», 77 P 2224444542] q K tatt. 1 Aur errr? fo {?] [Pe re # O| Tn ef Gq PRP A am SaY L LZ L 27 Base from U. S. Geological Survey Bagdad quadrangle, 1948 1 LE_L HIL LSIDE 22 Mi 0 i i 1 1 FIGURE 28.-Geologic map of Boulder Creek area, Yavapai County, Ariz. | Geology after C. A. Anderson, 1955 2 Miles ] LOCALITIES IN NEW MEXICO Precambrian rocks are schists, quartzites, and amphib- olites of the Yavapai schist that have been intruded by granite, gabbro, and a little quartz diorite. A stock (fig. 28) of Precambrian porphyritic biotite granite at Lawler Peak is about 3 miles in diameter. The rock is characterized by orthoclase phenocrysts as much as 2 inches in length. Small stocks of quartz monzonite intruded along a northeast-trending belt during Late Cretaceous or early Tertiary time. Pyrite, chalcopy- rite, and molybdenite occur in the quartz monzonite as disseminations and small fracture fillings which consti- ture the ore of the Bagdad and other mines. Tertiary conglomerates and basalt flows cover the earlier rocks in parts of the area. The tungsten-beryllium deposit is on the south side of Boulder Creek about 4 miles airline northeast of Bagdad (fig. 24), in see. 24, T. 15 N., R. 9 W. In the vicinity of the prospect the porphyritic biotite granite is highly altered, with destruction of the biotite and formation of muscovite and minor amounts of garnet and fluorite. Some beryl occurs as poikilitic inter- growths with the other rock minerals and seems to be related to the alteration. The wolframite-bearing veins are also in muscovite-rich granite. The wolframite oc- curs in closely spaced nearly vertical parallel quartz veins as wide as 1 or 2 inches. South of Boulder Creek the veins form a northeast zone nearly 12 feet wide and 200 to 300 feet long. On the north side of the creek, an east ward-trending zone of veinlets 10 to 50 feet wide can be traced for more than 2,000 feet. Beryl is an impor- tant accessory in the veins and locally is abundant. Some scheelite occurs in thin films and crusts on the surface exposures. The veins are thought to be related genetically to the granite stock. The vein zones were sampled by Anderson and his associates. A channel sample taken across the northern zone contained 0.16 percent WO; and 0.05 percent BeO, and a similar sample from the southern zone contained 0.13 percent WO; and 0.2 percent BeQ. Beryl is reported as a minor constituent of pegmatite dikes that are common in the porphyritic biotite gran- ite. It also occurs in the granite about 2,000 feet south- west of the wolframite-beryl prospect. Specimens from this locality consist of a granular mass of quartz and cloudy feldspar that contains about 30 percent beryl. The beryl is in euhedral prisms about 3 millimeters in diameter and 2 centimeters long, reticulated in all di- rections through the mass of quartz and feldspar. The beryl-bearing rock occurs in at least two tabular bodies, or "veins," 6 to 10 inches wide and 30 feet long, and averages 4.5 percent BeQO. The minerals associated with intrusions of Tertiary age at the Bagdad mine seem to have no beryllium. 107 According to Anderson (1950b, p. 618), the unaltered quartz monzonite contains less than 0.0004 percent BeQO. A biotite-albite-quartz-orthoclase facies of altered quartz monzonite associated with the Bagdad ore de- posits contains 0.0004 percent BeQO. Beryllium was not detected in samples taken at the Bagdad mine and other mines in Yavapai County for the Mine, Mill, and Smelter Survey during World War IL. NEW MEXICO By W. T. Honser The localities at which pyrometasomatic deposits and alkalic igneous rocks were sampled in New Mexico are shown in figure 29. Tactite deposits are known in many of the mining districts of New Mexico (Lindgren, Graton, and Gordon, 1910, p. 51-53) and nearly all of these were sampled. Samples of tactite from the cen- tral New Mexico iron districts were obtained through the courtesy of V. C. Kelley of the University of New Mexico. The deposits in the Juarilla district, Otero County, had been sampled previously by the American Smelting and Refining Co. According to L. K. Wilson of Tucson, district geologist for the company, the sam- ples contained little or no beryllium. The largest known reserves of nonpegmatite beryl- lium in New Mexico are in the tactite deposits at Iron Mountain (Jahns, 1944a; 1944b). Vein and tactite de- posits in the Victorio Mountains are also of potential importance. Small quantities of beryllium might be re- covered from deposits in the Carpenter and Apache districts. Phonolitic lavas of large areal extent in the Raton volcanic region contain as much as 0.007 percent BeQO, but the beryllium may not be recoverable. Alkalic igneous rocks were sampled in the Raton vol- canic region, Colfax County, and in the Cornudas Mountains, Otero County. The rocks of the Cornudas Mountains are related to those of western Texas and are described in the section dealing with the Trans-Pecos Region. caTRON CcoUNnTy BLACK RANGE DISTRICT Tin deposits of the Black Range are in Catron and Sierra Counties, on the western slope of the range, east of State Highway 61, about 50 miles north of Silver City, N. Mex. They were visited on August 22 and 23, 1949. The tin deposits, which have been described by Fries (1940), and Fries and Butler (1943), occur in a rhyo- litic volcanic series that contains some interlayered tuffs and breccias. Small veins that contain specularite and cassiterite and minor quantities of cristobalite, tridy- mite, fluorite, chalcedony, opal, and quartz occur in a 108 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 108° 106° 104° EXPLANATION ite Sntmniiett wre Sean terion, meh are _._._-—} e2 l Locality sampled for this report I l I x21 } € F Other sampling ( R E % 36° ——J| X.. "ese i {-- 36° I I 21 ____l I */. 6 \\ may l ANTA FE \ I [| I ". -_ I 1s fl & am | 22 *~ | | mB 4 I _H_, J" | | 1T f I, Ege - 1 ~- I 10 j | | Bess 108° 106° 104° 40 0 120 Miles i eal 1 1 ] DISTRICTS Catron County Hidalgo County Sandoval County 1. Black Range fl) fipalcllpte: No. 2 21. Cochiti . Hachita Colfax County 12. Lordsburg Santa Fe County 2. Cimarroncito 13. San Simon 22. New Placers 3. Elizabethtown ia Lincoln County 23. Old Placers 4. Raton volcanic region 15. (313.511 Iii-£1 3 @ 4 ele NSiirm County Dona Ana County una County . Apache No. 5. Organ 16. Tres Hermanas fig guehlfilo Nggyo a t County 17. Victorio . fron Mountain \ yaut Lou Otero County & Count §f gut-to flountams 18. Fuaritla Tif Y mocorro ounty . Carpenter a . Jones Ca: 8. Cenltfal (includes Hanover, Fierro San Miguel County P and Santa Rita districts) 19. Rociada ,___ Taos County 9. Pinos Altos 20. Willow Creek 28. Red River FiGuRE 29.-Index map showing localities sampled in New Mexico. LOCALITIES IN NEW MEXICO porphyritic rhyolite of the lower part of the series. Alluvial deposits near the veins are rich in placer cas- siterite. A grab sample (329-711) from a pit above the U. S. Bureau of Mines adit 1 N in the Taylor Creek area (Fries, 1940, pl. 55), contained 0.002 percent BeQ. The beryllium-bearing mineral was not identified. CcoLFaAx COUNTY CIMARRONCITO DISTRICT The Cimarroncito district is in the Cimarron Range in western Colfax County on land of the Philmont Scout Ranch. Eight miles of private road lead from the ranch headquarters on State Highway 21 to Cimar- roncito Camp (fig. 30). From there trails go up both the Middle and North Forks of Cimarroncito Creek to the mining area. The district was visited on July 19, 1949. e a ~;, at ~ £5 T;1’< 329-376 ¥ CirrEarrancito 3 ‘ f am y fl/*,\/‘ffi’pd\— roncifo a_. _. 329-382 a ' / F éw/ $ @ a o j g / (i yey 57 miLeS c it g EXL Creek. _- ' S?fl # x _- x 4 7". * EXPLANATION * 1 9 2 Miles a >- 329-382 x Shaft Adit Sample number FIGURE 30.-Sketch map of localities sampled in the Cimarroncito district, Colfax County, N. Mex. The mines of the district were described by Graton (Lindgren, Graton, and Gordon, 1910, p. 105-108). More recently the geology of the area was described by Smith and Ray (1943). Limestones of the Magdalena group of Pennsylvanian age are intruded by large sills and dikes of quartz-monzonite porphyry. North of the North Fork of Cimarroncito Creek, limestone of the Magdalena is overlain by Dakota sandstone and Pierre shale of Cretaceous age in the eastern limb of a large anticline. Near its contact with the porphyry, the lime- stone has been metamorphosed to tactite containing gar- net, epidote, diopside, and coarse calcite. Pyrite, specu- larite, magnetite, and chalcopyrite occur with some of the tactite. The approximate locations of the mines which were sampled are shown in figure 30. The mine on the North Fork of Cimarroncito Creek, from which sample 829- 382 was taken, is known locally as the Cypher mine. 109 Tt seems to best fit Gordon's description of the Thunder mine (Lindgren, Graton, and Gordon, 1910, p. 107- 108). The mine area on the north slope of the Middle Fork, from which samples 329-376 to 378 were taken, is probably the one known locally as the Lambert mine, but does not correspond to any mine described by Gordon. As the mines were not accessible, samples were obtained from dumps and outcrops as follows: 329-376 Chip sample from 15 ft of outcrop of garnet tactite at portal of upper adit. Grab sample of garnet-diopside tactite with pyrite, chalcopyrite, and specularite, from dump of lower adit. Grab sample of specularite-hornblende tactite with pyrite, chalcopyrite, calcite, and epidote ; same local- ity as sample 377. Grab sample of garnet tactite from dump of upper adit. (No tactite in dump of lower adit.) 377 378 382 Spectrographic analyses of the samples showed no more than 0.0004 percent BeQO. ELIZABETHTOWN DISTRICT The Elizabethtown district in western Colfax County is northeast of Eagle Nest, a small town on U. S. High- way 64. The geology of the district was described by Graton (Lindgren, Graton, and Gordon, 1910, p. 92-105), and that of the bordering Moreno Valley was described by Kelley (1949, p. 76-78). The principal sedimentary formation is the Pierre shale (Creta- ceous), which is capped on some of the peaks by the Raton formation of Cretaceous and Paleocene age. The shales are intruded by large sills and in some places by irregular bodies of quartz monzonite porphyry. Near the contact the shales have been metamorphosed mainly to a fine-grained hornfels, but in the vicinity of Iron Mountain, in the southwestern part of the district, coarse-grained tactite bodies containing epidote, specu- larite, magnetite, diopside, hornblende, garnet, and scapolite have been formed. Gold, the major metal pro- duced, has been mined principally from quartz-pyrite veins which are closely related to the intrusive por- phyry. Copper-gold deposits in the tactite are of minor importance. The specularite-epidote tactite bodies on the western slope of Iron Mountain have been pros- pected but never mined. The district was visited in June 1949. A description of the samples taken and the analytical results obtained are given in table 49. The iron-rich tactite on the west side of Iron Mountain and the copper-gold tactite de- posits in Willow Creek on the east side of the mountain were sampled. Two samples were taken at the Baldy Deep tunnel, one of the larger mines in the northern part of the district. 110 TaBus 49.-Beryllia in samples from the Elizabethtown district OCCURRENCE OF NONPEGMATITE B [Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] Sample Description (piecgnt) 329-262 Grab sample of quartz vein material with molybdenite in biotite granite, from dump of Baldy Deep tunnel.._.____._____ <0. 0004 263 - Grab sample of epidote-garnet tactite, from same locality as sample 262. ___ <. 0004 267 10-ft channel sample of epidote-specularite tactite from near portal of lower adit at Iron Mountain iron deposit.. _ <. 0004 271 20-ft channel sample of epidote-specularite tactite from portal of upper adit, same - _/ deposit as sample 267. .._______________ . 0004 272 Specimen of coarse specularite, from same locality as sample <. 0004 278 Grab sample from 25 ft of outcrop of diop- side hornfels in road cut on east side of Willow Creek above the Ajax mine.... <. 0004 274 Specimen of hornblende-diopside tactite from outcrop at the Ajax mine . _ _ __ __ __ <. 0004 275 Specimen of scapolite(?)-diopside tactite, from same locality as sample 274. <. 0004 RATON VOLCANIC REGION Volcanic cones and lava-capped mesas dominate the landscape throughout an area of about 1,500 square miles in Colfax and neighboring counties, adjacent to Raton (see fig. 31). Similarities of occurrence and com- position indicate that these volcanic rocks are of com- mon or related origin. Some of the rocks are analogous in their geological relations and composition to beryl- lium-bearing feldspathoidal rocks of the Trans-Pecos Region. The Raton region was visited in June and J uly 1949, and samples were obtained at several localities. Al- though the beryllium found in the volcanic rocks prob- ERYLLIUM IN THE UNITED STATES connection with the thesis that beryllium tends to be concentrated in feldspathoidal members of a rock series. GEOLOGY The general geology of the Raton region was de- scribed by Lee (1922) and Griggs (1948) ; detailed dis- cussions of the volcanic rock series are given by Collins (1949) and Stobbe (1949). The pre-Tertiary rocks are continental and marine strata of Mesozoic age, chiefly shale and sandstone but containing some limestone. De- tails of the stratigraphy are given in the publications cited. Earth movements in Tertiary time gave rise to the Raton basin and the Sierra Grande arch, which trends northeast across the center of the volcanic area. Planation of the deformed surface was followed by deposition of the Ogallala formation in Pliocene time. Later deformation, presumably related to the volcanic activity, in Quaternary time, gave the gravels a regional dip of about 50 feet per mile to the southeast. The sequence of lavas in the Raton region was worked out by Mertie (Lee, 1922, p. 9) largely on the basis of physiographic evidence. Later workers have given con- - flicting interpretations, particularly for the rocks in southern Colfax County (Griggs, 1948, p. 37-40; Col- lins, 1949, p. 1032-1036; Stobbe, 1949, p. 1071-1077). The probable relation of the volcanic rocks in the Raton area to rocks in the Cimarron Range to the west (Smith and Ray, 1943) is given in table 50. In essence, the age correlations and structural interpretations of Collins (1949), and Stobbe (1949), and the geologic boundaries mapped by Griggs, Northrop, and Wood (Griggs, 1948, ably is not recoverable, its distribution is of interest in pl. 1) are adopted for this report. The names applied 50.-Correlation of volcanic rocks and related units in the Raton region [Equivalent or correlative rocks are connected by dashed “neg Smith and Ray, 1943 (Cimarron Range) Mertie (in Lee, 1922, p. 1-12)(Raton- Brilliant-Koehler-quadrangles) Collins (1949) and Stobbe (1949) (Colfax and Union Counties) Quaternary rock names are those given by Collins (1949, p. 1022-1023) Griggs, Northrup,and Wood (in Griggs, 1948, pl. 1) (Colfax County) "Youngest lavas" (east of quadrangles)- f>-Late basalt flows - - - - Capulin basalts (flows). ry a E| Basalt lava flows and stocks - -- - t Intermediate mafic flows -- - £ | Clayton basalts (flows, minor dikes) § 5 (with mafic dikes,in part). § ke 3 if Andesite flows and stocks -- --- I Intermediate felsic flows & |,Chico phonolites (flows, minor § é ba. dikes, and sills). $ x / Slagle trachytes (sills, minor 6 € y 335.3 Basalt, rhyolite, and dacite (Urraca-|-Basalt lava flows __ )\ dikes). & & Mesa). r sg P / Red Mountain dacites (flows, minor A A a_ fs , / i [/ dikes). § Gravels (including Eagle Nest- -- | High-level gravels (in part) w z E>Early basalt flows (with / Raton basalts (flows, minor dikes) ® - formation) Xv 3" mafic dikes, in part). / A @ L 0 3 aem "To 4 g / 5 P. Basalt (in part - La Gruilla Mtn.)--| Basalt lava flows -~ ~~ 8 ,~»Ogallala formation / / g Ogallala formation _-3 8 : ane a" High-level gravels (in part) ~~ E 3 / A ; ap # £ $ { f ©8 Quartz monzonite porphyry sills Az 4 2 is as o sake maak -B I Sills and dikes Basic dikes § Guarte monzonite porphyry $ - and dikes (southwest of quad- & 5 a 2s T q - rangles). ye 8, < LOCALITIES IN NEW MEXICO 111 105° 104° 103° L -A S As colorado. {szo N EW | MEX1C O 1 ( J bs 0 a T <4 ; 3 Cc=o _ L__F . A: Fes r.-- [ U 36° 36° w < 1 | X I u m 1-6 (U e L 1g O Las Vegas *% \\ f | \ | 105° 104° 03° Modified polyconic projection I After Collins (1949), Griggs (1948), Smith and Ray (1943), Ray and Smith (1941), and Darton (1928) FIGURE 31.-Map of post-Cretaceous volcanic rocks of the Raton region, New Mexico. to the rocks are those suggested by Collins (1949, p. 1022-1023). Three ages of basalt flows have been recognized. The oldest flows, the Raton basalts of Collins (1949), cap the high mesas near Raton. They are gray, fine- grained, vesicular rocks with olivine phenocrysts. The basalts of intermediate age, the Clayton basalts of Col- lins (1949), occur at lower altitude. They contain olivine phenocrysts, and a few of the flows are felds- pathoidal. The youngest basalts, the Capulin basalts of Collins (1949), generally are in the valleys. They are black, dense to vesicular rocks with large feldspar phenocrysts and some olivine. The major differences of opinion concern the volcanic rocks other than basalt. These include the Red Moun- tain dacites, Chico phonolite, and Slagle trachytes, all of Collins (1949), which are mainly around volcanic centers in southeastern Colfax County. - Collins' Red Mountain dacites are apparently equivalent to the "intermediate felsic flows" of Griggs, Northrop, and Wood, which they correlate with Collins' Clayton ba- salts. According to Collins (1949, p. 1032), the boun- dary relations between his Red Mountain dacites and his Clayton basalts indicate that the latter is younger. He assumes from physiographic and petrologic data that his Chico phonolites and his Slagle trachytes are closely related rocks that fall into the same age bracket (post-Raton and pre-Clayton) as the Red Mountain 112 dacites. Apparently, the phonolite and trachyte cor- respond to rocks referred to by Griggs, Northrop, and Wood as "sills and dikes" of early (?) Tertiary age. Although there is general agreement that the trachytes are largely sills, Collins (1949, p. 1034) states that the phonolites are mainly flows, with few sills and dikes. The phonolite is a green to gray, fine-grained rock containing phenocrysts of aegirite and feldspar. The groundmass is composed of nepheline, analcite, ortho- clase, and aegirite, with accessory sodalite, magnetite, and sphene. The trachyte is light brown, fine grained, and contains sparse feldspar phenocrysts. The ground- mass is mostly orthoclase, with some acmite-diopside and barkevikite. OCCURRENCE OF BERYLLIUM All of the major volcanic rock types were sampled, mainly in the vicinity of the volcanic centers in south- REBE. R.26 E. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES eastern Colfax County. Most of the samples were chipped at intervals across fresh outcrops; in a few places carefully selected hand specimens were taken. The localities sampled are shown on figure 32, and ana- lytical data are given in table 51. The Chico phonolites of Collins (1943) and related dikes are the only rocks in which beryllium was found. These rocks are confined to an area of about 25 square miles in southeastern Colfax County (fig. 32). Most of the phonolite is associated with volcanic centers at Turkey Mountain and Temples Peak. Sills and dikes in the Slagle Canyon area, a few miles south of Turkey Mountain, are similar to the phonolite and probably related to it. The distribution of BeQ in the rocks appears to cor- relate roughly with the zirconium content, and an in- verse relation to the chromium content is suggested. There is also an apparent correlation between BeQ con- R.27E. EXPLANATION SEDIMENTARY ROCKS TERTIARY AND z Pliocene and Recent QUATERNARY Undifferentiated units IGNEOUS ROCKS 7 + ~ TimegR s .¢ch 329-364; 0.002 329-365; 0.002 «Milk, Ca N 10 m NO mes 329-360; 0.002 329-367; <0.001 329-369; 0.007 AME + a x2 329-372; < 0.00 sx Kt, im 1 ~ _ srare se W’\ | 329-373; < 0.001 Capulin basalts A & 3 © [(A »Qc e ¥. ‘, T '-VJA.'\;'.< 27? Clayton basalts esas. 1 . Ta QUATERNARY Chico pl es and Slagle trachytes +0 + + + # + , Qrm , Ls. +0 + + + Red Mountain dacites gt FSSS T. Raton basalts J "y 26 B s +" e" Names are those used by Collins, 1949 Contact 329-373; < 0.001 Locality sampled; percent beryllia 2 0 B63 214024 | AIMiIes After Griggs, 1948, and Collins, 1949 FIGURE 32.-Map of volcanic rocks of southeastern Colfax County, N. Mex. LOCALITIES IN NEW MEXICO 113 TaBu® 51.-Beryllium and other elements in volcanic rocks of the Raton region Percent Rock type } Sample No. Sample type Description BeO ? Cr: Zr eU $ U4 Capulin basalts... - 329-372 Hand specimen from Highly vesicular black <0.001 0.00X 0.00X <0.001. .._... flow surface. basalt. Clayton 867 t-. _.Uo 2 -can Grgy film-grained <.001.. . OX . OOX - = a 4 in 7 s* >) LC £) \ Rea" "/a is z u* 4E Wz +5 X it ; Quartz monzonite < vs TuS u +4 Aip bmp ar 0. hal. Ad as {2 s= es Amf C \\’\H=I(\\’:\ '.~.'~~'>‘l/\ El er z REY a2. =s Tals, T - 4Tm‘:u/\\; \& V Q‘KC % 27 - §21 =, _I/://“ waz > 17/0 #*, ¢\\(\“:‘ \ Volcanic breccias and flows f td> S s RANDVIEW MIN Xess C V agilh + year d. \ w w w \ < 4 a \ Lake Valley limestone < SQmf. z © \\ x Dp 5 > a s Percha shale TRUE NORTH SOmf Montoya and Fusselman limestone, undifferentiated u oep ::. X_ _- ( N--y_- ORDOVICIAN ORDOVICIAN DE El Paso formation Coma—“i A Dashed where inferred a2 e quite mente Fault, showing dip Dashed where inferred >-- Portal of adit OLUMBIA MINE J Glory hole Other mine workings Geology by R. L. Griggs and S. P. Ellison, U. §. 0 for ological Survey unpublished map, 1943 3C}00 Feet -O | | FicurE 33.-Geologic map of part of the Carpenter district, Grant County, N. Mex. 115 PIAN AND SILURIAN 116 GRANDVIEW MINE The Grandview mine is in sees. 29 and 32, T. 16 S., R. 9 W., 15 miles by road northeast of State Highway 61. The claims had been prospected for about 50 years before the first shipment of lead-zinc ore was made in 1937. From 1938 to 1945 the mine was developed by the Black Range Development Co., and about 19,000 tons of ore, including 1,600 tons of zinc, 900 tons of lead, 46 tons of copper, and 14,000 ounces of silver were produced. The mine was idle from 1945 until 1948, when small shipments of ore were made to the Black- hawk custom mill at Hanover, N. Mex. In August 1949, the mine was not operating. Development of the mine has been mainly through two adits at altitudes of 7,516 and 7,570 feet; several stopes connect with a glory hole at about 7,625 feet altitude. A winze goes a short distance below the 7,516- foot level, A short adit was driven about 250 feet south of the portal of the lower adit. Helvite from the Grandview mine was first discov- ered by J. W. Adams on a specimen of fluorite collected by A. E. Weissenborn, both of the Geological Survey. During the present investigation several specimens of helvite were collected, both from the dumps and from small veins exposed in the glory hole. The refractive index of the helvite is variable but is near 1.730 (Weis- senborn, 1948, p. 649) ; this indicates that it is essen- tially the manganian member of the series (Glass, Jahns, and Stevens, 1944, p. 183). The helvite occurs mainly in vugs lined with small prisms of quartz, mostly in cherty limestone. Many of the quartz crys- tals are coated with a thin layer of chalcedony. Crys- tals of fluorite and sphalerite are later than the quartz. Tetrahedra of helvite as much as 3 mm on an edge grow in or on the chalcedony but not on the quartz crystals. Some of the helvite is associated with fluorite, but a sample of the fluorite contained no beryllium. Samples were taken from the dumps and under- ground workings at the Grandview mine, as described in table 54. No beryllium-bearing minerals other than helvite were found in the samples, and it is assumed that almost all of the beryllium is contained in helvite. The possibility of byproduct recovery of beryllium therefore appears to be good if the mine returns to operation as a lead-zine producer. Beryllium was not found in a garnet-rich sample (829-717) from the southern adit. This may indicate that the occurrence of beryllium at the Grandview mine is not related to pyrometasomatism. The association of helvite with chlorite and chalcedony in vugs suggests deposition at relatively low temperature. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 54.-Beryllia in samples from the Carpenter district {Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] BeO Sample (percent) 329-315 712 TIT 718 Description Specimen of white fluorite from dump of lower adit, Grandview mine__._______ Channel sample of rhodochrosite-galena vein,-same Grab sample of garnet-galena ore from southern adit, Grandview mine...... Grab sample of vuggy quartz vein ma- terial, with galena, sphalerite, and fluorite, from upper adit of Grandview ming. . No helvite seen_______:_....__ . 02 Channel sample of highly oxidized ma- terial, with chlorite, galena, and hema- tite, from short abandoned adit just north of main upper adit, Grandview mine. 0C 02) dlc .s. . 02 Channel sample of limestone highly al- tered to chlorite, with iron and manga- nese oxides; same location as sample pl e oil a apa art e sal Channel sample of cherty limestone with vugs containing quartz, galena, and helvite, along north-trending vein in glory hole of Grandview mine. . O1 Grab sample of andradite-diopside banded tactite, with epidote, from dump of Columbia Specimen of sphalerite-galena-fluorite ore from dump of Columbia mine________. Composite sample of mill heads for 2 days in May and June 1949, from Grandview mine (Blackhawk mill, Hanover) ._.... - O1 0. O01 . O01 x. BOL 720 721 <. 001 722 726 . 001 <. 001 727 7835¢ OTHER MINES The Columbia mine is about 4,000 feet south of the Grandview mine (fig. 33). About 600 feet of drifts explore small veins in the Montoya limestone. Samples of tactite and of sphalerite-galena-fluorite ore taken from the dumps contain less than 0.001 percent BeQ (table 54). CENTRAL DISTRICT (INCLUDING FIERRO, HANOVER, AND SANTA RITA DISTRICTS) The Central mining district, about 15 miles east of Silver City, covers a large area between Bayard and Fierro, N. Mex. The principal mines are large pro- ducers of copper, zinc, lead, and iron. During the pres- ent investigation, the area was visited in J uly and August 1949. Several geologists with experience in the region furnished information and samples. Thanks are due especially to S. G. Lasky and R. M. Hernon of the U. S. Geological Survey, Harrison Schmitt, consulting geologist, of Silver City, and geologists and engineers of the American Smelting and Refining Co., Empire Zinc Co., Kennecott Copper Co., and Peru Mining Co. The complex geology of the district has been the sub- ject of much study ; the numerous published reports in- clude those by Lindgren, Graton, and Gordon (1910, p. 305-317), Paige (1916), Landon (1931), Schmitt (1935, 1939), Spencer and Paige (1935), Lasky (1936), Lasky LOCALITIES IN and Hoagland (1948), Hernon (1949), Kelley (1949, p. 83-124), Graf and Kerr (1950), and Kerr, Kulp, Pat- terson, and Wright (1950). The district is on the Fort Bayard arch, which modifies the eastern limb of a broad syncline of sedimentary rocks of Paleozoic and Mesozoic ages. At various times the sediments were in- truded by stocks, sills, and dikes of a variety of igneous rocks. Early quartz diorite sills are conspicuous; one known as the Marker sill is found in the Magdalena formation of Pennsylvanian age throughout most of the district. The principal intrusive body is the Han- over granodiorite stock, about 214 miles long; the smaller intrusives at Santa Rita and Copper Flat are of similar age and composition. Related granodiorite dikes of at least two ages were intruded along steep northeast-trending faults. Thermal metamorphism has been widespread and in most places was accompanied by large additions of ma- terial. Andradite, hedenbergite, magnetite, and ilvaite are the principal minerals in tactite bodies formed around the southern end of the Hanover stock and at Copper Flat, where they replace the Lake Valley (Mis- sissippian), and the Magdalena (Pennsylvanian) lime- stones. The occurrence of tactite is controlled by dike- fault zones and favorable stratigraphic horizons, as well as by nearness to the intrusive body. Epidote is common in shaly members. The lower limestones of early Paleozoic age, particularly the El Paso (Ordovi- cian) limestone at Fierro, are principally replaced by magnetite, serpentine, and wollastonite. Small amounts of magnetite and garnet occur along the northern border of the Santa Rita stock. Garnet and pyroxene are found in a few places along the dike com- plex that extends southwestward toward Vanadium. Many of the ore deposits are associated with the tactite bodies. In the Hanover area large masses of sphalerite replace the tactite along its contact with the unsilicated marble, particularly in the upper member of the Lake Valley limestone. These deposits are repre- sented by samples from the Empire Zine Company quarries and from the Pewabic mine. At Copper Flat similar deposits occur within the tactite. Between the Hanover and Santa Rita stocks, sphalerite bodies lie along north-trending fissures. The gangue contains hedenbergite and a little garnet, ilvaite, thodonite, and epidote, as well as calcite. Although the deposits are not close to intrusive rocks, they are probably similar in origin to those of the Pewabic and Empire zinc mines. This type of deposit is represented by samples from the Oswaldo mine. In the southeastern part of the district, near Vana- dium and Bayard, sphalerite-galena-chalcopyrite ore occurs along the contacts of the granodiorite dikes with 117 NEW MEXICO Upper Cretaceous shale and limestone. Although both the dikes and the shale were extensively replaced by quartz, sericite, and pyrite, silicates such as pyroxene and garnet are much less common. This type of deposit is represented by the Ground Hog mine, where samples were taken mostly from the rare garnet-pyroxene zones. The large copper deposit at Sana Rita is a replacement of the granodiorite stock, and was not sampled. The samples taken are described in table 55. Ap- parently the large tactite bodies at the southern end of the Hanover stock, both on the western side (Buck- horn Gulch and Hill 6650) and on the eastern side Tasug 55.-Beryllia in samples from the Central district [Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] BeO (percent) Sample Description 329-276 4-ft channel sample of hedenbergite-gar- net-calcite marble from top of Lake Valley limestone in Uncle Sam quarry, Buckhorn Gulch, 8-ft channel sample of epidotized shale (so-called Parting shale of local usage) from base of Oswaldo formation, Mag- dalena group, from same locality as sample Chip sample from 50-ft exposure of garnet tactite, lower part of Oswaldo forma- tion at south end of "150 quarry," Buckhorn Gulch: S-ft channel sample of magnetite-garnet tactite from Oswaldo formation in iron mine at top of Hill 6650, 4 mile west of ues Chip sample from exposure of garnet- hedenbergite tactite in Oswaldo forma- tion above white marble and below epidotized shale, "350 quarry," Buck- horn Chip sample from 125-ft exposure of gar- net tactite in Oswaldo formation be- tween Hanover stock and Hanover sill, in road cut 800 ft south of Hanover... Chip sample from 20-ft exposure of mag- netite-garnet tactite in upper part of Lake Valley formation, open pit of Snowflake fron mine._______-__-------- Chip sample from 6-ft exposure of mag- netite-serpentine in so-called parting shale of local usage of Oswaldo forma- gigs, from same locality as sample 329- Chip sample from 2-ft bed of garnet-py- roxene bhornfels in upper part of Abo sandstone, near Mountain Home mine on Humboldt Mountain. Idocrase re- ported from this locality (Schmitt, 1939, p. 812) but none was noted in the sampling. Specimen of rhodonite- and hedenbergite- bearing limestone from 445N stope of Oswaldo Core split of garnet-diopside tactite, with pyrite, magnetite, chalcopyrite, and sphalerite, in Oswaldo formation, from 41 to 302 ft in diamond-drill hole 1101, Santa Rita Core split of garnet-pyroxene-epidote tactite and some hornfels, with pyrite, magnetite, and chalcopyrite, in upper part of Lake Valley limestone, from 320 to 590 ft in diamond-drill hole 1101, Santa Rita area..-..c...l.-.._...:.s.- <0. 0004 277 . 0008 280 . 0004 281 . 0004 282 <. 0004 284 . 0004 286 . 0004 287 . 0004 288 . 0004 289 . O0OX 291 <. 0004 292 <. 0004 118 55.-Beryllia in samples from the Central district-Con. BeO (percent) Sample Description 293 Core split of epidote-chlorite-pyrite-ser- pentine rock, with some massive biotite hornfels, in lower part of Lake Valley limestone, from 590 to 685 ft in dia- mond-drill hole 1101, Santa Rita area. Core split of 6 in. out of 15.5 ft of highly altered granodiorite dike in Lake Valley limestone, from horizontal drill hole east of 436 drift in Oswaldo mine_____ Core split of 7 in. out of 12.5 ft of epidote- garnet-pyrite tactite from same forma- tion and drill hole as sample 294._____ Core split of 5 in. out of 1.5 ft of sphalerite and tactite from same formation and drill hole as sample 294._.___________ . O01 Core split of 5 in. out of 10 ft of unmeta- morphosed limestone, same formation and drill hole as sample 294._._______ Chip samgle from 50-ft exposure of garnet and sphalerite in lower part of Lake Valley limestone on 160 level Pewabic MiflG ck - 1 mus c - nea hr se cums dad ane col <. 0004 6-ft channel sample of garnet-diopside tactite in upper part of Lake Valley limestone on 160 level of Pewabic TiNC . .? s nen bee uae e elan b dn oue oh aar wh <. 0004 6-ft channel sample of garnet tactite in upper part of Oswaldo formation, on 160 level of Pewabic <. 0004 Grab sample from _ 500-sq-ft exposure of granodiorite of Hanover stock, 1,000 ft east of Hanover. - Aplite dikes excluded from sample...... 3.0200 01.00}; <. 0004 80-ft channel sample of magnetite-ser- pentine tactite highly altered to clay, from upper part of El Paso limestone at northwest end of open pit at Jim Fair mine, OL c_ :o <. 0004 Grab sample from 2,000-sq-ft exposure of garnet tactite in Oswaldo formation, west side Yellowdog Gulch, near west edge of Copper Flat stock. Idocrase reported from this locality (personal communication from R. M. fiernon) but none was found during sampling . _ 730 4.5-ft channel sample of hedenbergite tactite altered to chlorite, with sphal- erite, in upper part of Lake Valley lime- stone near quartz granodiorite porphyry dike on 1,800 level of Groundhog mine. . O01 Specimen of hedenbergite and sphalerite- pyrite ore, in upper part of Lake Valley limestone near hornblende granodiorite porphyry dike 25 ft above 1,800 level of Groundhog mine. .c }}}; 733 4-ft channel sample of hematite-pyrite- sphalerite-hedenbergite tactite at con- tact of quarts granodiorite porphyry dike and limestone, 1,800 level of Groundhog Grab sample from 4-in. vein of rhodonite- sphalerite-hedenbergite in limestone near quartz granodiorite porphyry dike on 1,800 level of Groundhog mine____ . Grab sample! of garnet (GrogAnssAlyq)- hedenbergite tactite with sphalerite, at dike contact on 1,800 level of Ground- hog _ _ . 002 ! Sample collected by Mr. B. C. Hardie of American Smelting & Refining Co. gua <0. 0004 208 . 0004 206 <. 0004 207 sof <. 0004 302 303 305 306 308 <. 0004 732 - 0008 . 0008 734 f <. 0004 80 (Pewabic mine), contain little or no beryllium. The same is true of the magnetite deposits farther north (Snowflake and Jim Fair mines). Small amounts of beryllium were detected in the limestone replacement OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES ores of the Ground Hog and Oswaldo mines. The highest value-0.002 percent BeO-was found in garnet tactite from the Ground Hog mine, but such material is quite rare in this part of the district. PINOS ALTOS DISTRICT The Pinos Altos district is in the Pinos Altos Mountains about 8 miles north of Silver City. The dis- trict was visited on August 24, 1949. James Neumann, chief geologist for the United States Smelting and Re- fining Co. at Vanadium, N. Mex., supplied specimens of the ores and information concerning the mining operations. The geology of the Pinos Altos district was described by Graton (Lindgren, Graton, and Gordon, 1910, p. 297-301) and by Paige (1910; 1916, p. 14). On the west side of the Pinos Altos Mountains is a north- trending mass of limestones of Paleozoic age about 1% miles long and less than a mile wide. Early mafic intrusive rocks, principally diorite porphyry, are cut by a mass of granodiorite about 2 miles in diameter. Both the main intrusive and diorite porphyry dikes cut the limestones and are accompanied by some pyrometa- somatic alteration. Tactites composed of garnet, pyrox- ene, and epidote are of limited and irregular extent. The ore is composed of sphalerite, pyrite, chalcopyrite, bismuthinite, and quartz; at places it occurs in the tactite. Both thrust and normal faults are common and some faults are mineralized. The largest mine in the western part of the district is the Cleveland tunnel, described in detail by Paige (1910, p. 122-125). A grab sample (329-738) of spha- lerite-pyrite ore collected from the dump contained less than 0.0004 percent BeQ. Although Graton (Lind- gren, Graton, and Gordon, 1910, p. 300) describes much garnet and specularite from this tunnel, none was ob- served on the dump. At the Houston-Thomas mine, which adjoins the Cleveland tunnel on the northwest, some garnet-pyroxene-epidote tactite was found. A. grab sample (329-740) of sphalerite-pyrite-chalcopy- rite ore from the dump of the new shaft of this mine contained less than 0.0004 percent BeQ. The geology of the mine is described in a report by Soule (1948). The gold-quartz fissure veins in the granodiorite of the eastern part of the district were not sampled. HIDALGO COUNTY APACHE NO. 2 DISTRICT The Apache No. 2 district is in the Apache Hills, 6 miles southeast of Hachita, N. Mex., which is on the Southern Pacific Railroad and State Highways 9 and 81. The district is reached by an unimproved road from Hachita. It was visited on August 26 and 27,1949. Al- LOCALITIES IN NEW MEXICO bert Fitch of Hachita, owner of the Apache mine, fur- nished much information on the deposits of this and - neighboring districts. Little work seems to have been done in the district since 1938 when the United States Smelting and Refining Co. ceased operations at their new shaft on the Apache claim. The geology of the district was described briefly by Lindgren (Lindgren, Graton, and Gordon, 1910, p. 343-344). Gently-dipping Cretaceous and possibly Pennsylvanian limestones are exposed in the northern part of the Apache Hills (Darton, 1928, p. 348). A sill- like intrusive body of granodiorite porphyry crops out along the southern slope of the hills. Ore deposits are found only at the southern contact of this body with limestone and consist of large masses of marble and tactite that are partly replaced by iron, copper, bismuth, and silver minerals. The ore minerals have been oxi- dized to a depth of at least 500 feet. Scheelite and wolframite are reported to occur in large quantities in part of the Apache mine. Four samples were taken at localities shown in figure 34 and are described below : Sample Description 329-752 Chip sample from 15 ft of exposure of garnetizéd mar- ble, with copper and iron stains, in face of glory hole 125 ft N. 20° W. of Apache shaft. Scheelite reported at this locality. 755 Grab sample of garnet-epidote-calcite—pyrite marble from dump of new Apache shaft. 781 Grab sample of garnet tactite from two lenses ex- posed in limestone and conglomerate. 783 6-ft channel sample of garnet tactite, with copper and iron stains, in limestone (sample 781 from same layer). Spectrographic analysis by Janet D. Fletcher did not detect beryllium in these samples, the limit of detection being about 0.0004 percent BeQ. HACHITA DISTRICT (INCLUDING EUREKA AND SYLVANITE DISTRICTS) The Hachita district is in the Little Hatchet Moun- tains about 12 miles southwest of Hachita. The mines in the northeastern part of the range, near Old Hachita, commonly known as the Eureka district, are reached by a graded road from Hachita. This part of the district is in Grant County. The mines in the southern part of the range, including the old camp of Sylvanite, are best reached over a road leading southwestward from Hachita across a pass in the Little Hatchet Mountains. The road along the southwestern part of the range south of Sylvanite was barely passable when the district was visited on August 25 and 26, 1949. An account of the geology of the Little Hatchet Mountains by Lasky (1947) contains excellent descrip- £19 3) f A \ 3 pap ry /) ',{,..'/\j' 4 ea I, _ true north Me MAG~E:TIC G % NORTH -C- 31° 50° BD 8 EXPLANATION , 329-752 ) Locality sampled and number. | rT All samples less than 0.0004 +~2_ 's 2 Yos | 7F \ i a cA \ percent beryliia ._.. _. 4, f-ghj C _5\”3(\s Hachita quadrangle, 1918 _| f aes u 108°15 1 0 l (22A 1 | I Contour interval 25 feet Datum is mean sea level 2 Miles ned FicurE 34.-Index map showing localities sampled in the Apache No. 2 district, Hidalgo County, N. Mex. tions of the metamorphism and mineral deposits in the area. The sedimentary rocks of the Little Hatchet Mountains are of Early Cretaceous age (Bisbee group), and include possibly 5,000 feet of the Broken Jug lime- stone overlain by about 15,000 feet of clastic sediments and volcanic rocks. The several intrusive bodies are mostly of Late Cretaceous or early Tertiary age.. Out- crops of monzonite and quartz monzonite near Eureka and Sylvanite are interpreted as being segments of a large continuous sill-like body in the sedimentary rocks. The rocks are displaced by the Copper Dick fault which down drops the northern half of the range by 3 miles. A stock of granitic rocks forms the southern tip of the range where dikes are common. Near their contact with the stock, the sedimentary rocks are metamorphosed to tactite and hornfels con- taining garnet, pyroxene, scapolite, and feldspar. A zone of actinolite marble occurs at greater but variable distances from the contact. The few short veins are mostly within or near the monzonite at Eureka and Sylvanite. At Sylvanite na- tive gold occurs with chalcopyrite, hessite, tetradymite, arsenopyrite, and pyrite in a gangue of tourmaline, ac- tinolite, quartz, and calcite. At Eureka galena and sphalerite are in a gangue composed chiefly of man- ganosiderite. Scheelite and molybdenite are un- common. 120 The following samples from the Hachita district were analyzed for beryllium: Sample Description 329-7402 Sample from several 8-in. channels across vein of scheelite-hematite-tetradymite ore at contact of monzonite and marble, from 25-ft shaft 200 ft south of the southeast corner of the Virginia claim (Lasky, 1947, p. 67). 4-ft core of mill tailings at American mill. Grab sample of arsenopyrite-pyrite-sphalerite~ manganosiderite-calcite ore, from dump of Ameri- can mine. ) Grab sample of manganese carbonate and oxides from dump of American mine. Chip sample from 100 sq ft of garnet-pyroxene tactite exposed northeast of Fitzgerald shaft, American mine. Chip sample across 30 ft of garnet-quartz tactite exposed north of Fitzgerald shaft, American mine. Grab sample of chalcopyrite-garnet ore from dump of Copper Dick mine. 20-ft channel sample of garnet tactite, with copper carbonates, from northeast face of opencuts at Copper Dick mine. 5 Sample of oxidized ore from Santa Maria tunnel, originally consisting chiefly of quartz, calcite, barite, chalcopyrite, pyrite, molybdenite, and epidote. Grab sample of garnet-chalcopyrite-molybdenite ore from metamorphosed Broken Jug limestone at contact of monzonite stock, on Wyoming claim northwest of Hachita Peak. Chip sample from outcrop of coarse amphibole tac- tite, from Howells Ridge formation near monzonite contact, south side of Sylvanite Gulch. res (42 743 744 745 746 revd 749 750 751 Spectrographic analyses by J. D. Fletcher did not detect beryllium in any of these samples, the limit of de- tection being about 0.0004 percent BeQ. The gold- quartz veins of the Sylvanite area were not sampled. LORDSBURG DISTRICT The Lordsburg mining district, also known as the Virginia district, is in the northern Pyramid Moun- tains, a few miles southwest of Lordsburg, which is on the Southern Pacific Railroad and U. S. Highway 80. The district was visited on July 25, 1949. The geology of the district was described in detail by Lasky (1988) and that of the fluorspar mines by Rothrock, Johnson, and Hahn (1946, p. 104-108). The oldest rocks are basalts of Early Cretaceous age, in- truded by plugs of basalt and rhyolite. An irregular stock of granodiorite forms the northeastern part of the mountains. Faults in the granodiorite which trend from east to northeast are the loci of the ore deposits. The most important veins contain chalcopyrite, galena, pyrite, and specularite in a gangue of quartz, calcite, and tourmaline. The earliest stage of vein formation included intensive replacement of the granodiorite wall rock by sericite, chlorite, calcite, tourmaline, and specu- OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES larite. Fluorspar was deposited with calcite and quartz in open fissures during a late stage of mineralization. Samples were taken in the Lordsburg district as de- scribed below: Sample 329-421 Description 3-ft channel sample across quartz-gossan at outcrop of "85" vein. Grab sample of quartz-sericite-tourmaline vein ma- terial with minor chalcopyrite, in granodiorite, from dump of "85" mine. Grab sample of quartz-specularite-chalcopyrite ore in basalt, from dump of "85" mine. Channel sample across 2.5-ft vein of fluorite, 30 ft northeast of Fluorite (Kneyer) No. 1 shaft. (See Rothrock, Johnson, and Hahn, 1946, p. 105-106.) Grab sample fluorite-calcite ore from outcrops and dumps of Fluorite No. 8 claim. 426 Same, from Fluorite No. 9 claim. Spectrographic analyses by J. D. Fletcher showed no beryllium in any of the samples. The samples from the "85" mine were analyzed qualitatively with a limit of detection of about 0.0004 percent BeQO, and the sam- ples from the Fluorite claims were analyzed quantita- tively with a limit of detection of about 0.0001 percent BeQO. Samples collected in 1943 from the Bonner mill in Lordsburg, which was treating ores from the Bonney and Anita No. 1 mines, for the Mine, Mill, and Smelter Survey of the U. S. Geological Survey also showed no beryllium, the limit of detection being 0.001 percent BeQ. Analysis of samples collected in 1943 showed 0.003 percent BeQ in the fluorite of the Kneyer No. 1 mine, but the analysis obtained for sample 329-424 is probably more reliable. 422 423 424 425 SAN SIMON DISTRICT The San Simon district is in western Hidalgo County, next to the Arizona boundary. It is in the southern part of the Peloncillo Mountains between Steins Pass on the north and Antelope Pass on the south. U. S. Highway 80 crosses Granite Gap about 2 miles north of Antelope Pass. An unimproved road leading south from the highway at the west end of Steins Pass pro- vides limited access to the district. Part of the district was visited on July 25, 1949. The geology of the district was described briefly by Lindgren and Graton (Lindgren, Graton, and Gor- dor, 1910, p. 329-332). The principal operation in 1949 was the Silver Hill mine. It is at the head of a canyon on the western slope of the mountains, 4 miles directly east of New Mexico-Arizona boundary monument No. 334 and 5 miles south of Steins Pass. This part of the mountains is composed of a thick section of gray thick- bedded limestone that dips 25° to the north; according to Graton (Lindgren, Graton, and Gordon, 1910, p. 331) it is probably Carboniferous in age. A monzonite porphyry dike 150-feet thick trends southwest for sev- LOCALITIES IN eral miles. Garnet, galena, and sphalerite replace lime- stone in the contact zone near the dike. About 500 feet north of the Silver Hill shaft, an aplitic branch of the dike strikes S. 50° W. Several hundred feet from the main dike the contact zone along the aplite branch has been explored by a 30-foot adit on the S and W claim. The ore here is similar to that at the Silver Hill mine. Two unidentified silicates, one of which resembles wol- lastonite, form part of the gangue at this locality. About half a mile south of the Silver Hill mine the workings of the Johnny Bull mine explore a similar dike contact zone. Garnet, quartz, and possible wol- lastonite and pyroxene are accompanied by pyrite, chal- copyrite, bornite, and oxidized copper and iron minerals. A 4-foot channel sample (329-427) was taken across the ore near the collar of the Silver Hill shaft and a 5- foot channel sample (329-429) was cut across the ore at the portal of the adit on the S and W claim. A sample of tactite (329-433) was chipped from a 10-foot exposure in an open pit below the north shaft of the Johnny Bull mine. Spectrographic analyses by J. D. Fletcher showed no beryllium in any of the samples, the limit of detection being 0.0004 percent BeOQ. LINCOLN COUNTY CAPITAN DISTRICT The Capitan iron-mining district is at the western end of the Capitan Mountains, just east of State High- way 48, 6 miles north of Capitan. Although time did not permit a visit to the district, a sample of contact metamorphic rock was furnished by V. C. Kelley, who had been studying the iron deposits for the U. S. Geo- logical Survey and the New Mexico Bureau of Mines and Resources. According to his report (Kelley, 1949, p. 144-153), a large stock of granite aplite intrudes the San Andres formation of Permian age. The main iron deposit is a ring-shaped body in the limestone mem- ber of the San Andres formation about 2,000 feet west of the contact with the granite. Structural relations suggest that the ore was localized in a pre-intrusion sink hole or collapse structure. An inner zone of epi- dote, phlogopite, and tremolite is surrounded by a phlogopite-tremolite zone, with magnetite concentrated toward the outside. The sample (329-810) collected by Kelley was from the outer part of the phlogopite-tremolite zone, between magnetite ore and limestone. The locality is shown in the lower center of his figure 25 (Kelley, 1949) as the northernmost of a pair of trenches just west of the Capitan road. Spectrographic analysis by J. D. Fletch- er indicated 0.005 percent BeQ. Further sampling for beryllium in this area seems warranted. 467945-59--9 NEW MEXICO 121 GALLINAS DISTRICT The Gallinas district occupies about 10 square miles at the eastern end of the Gallinas Mountains in north- ern Lincoln County. The area is served by U. S. High- way 54 and by the Southern Pacific Railroad at Gal- linas siding, 8 miles east of the district. Although time did not permit a visit to the district, samples were furnished by V. C. Kelley of the University of New Mexico, and R. G. Knickerbocker of the U. S. Bureau of Mines. E The geology of the district is described by Kelley, Rothrock, and Smalley (1947). Precambrian granite and gneiss are overlain by sandstone and siltstone of Permian age. In early Tertiary time these rocks were intruded by laccoliths and sills of syenite porphyry, with some monzonite and monzonite breccia. The rocks were cut by faults and breccia zones. Ore deposits of magnetite and of fluorite-barite-calcite-bastnaesite with minor amounts of sulfides, occur in the fractures and breccia zones. Locally, as at the American iron mine, epidote and tremolite are associated with the ore. Sample 329-808 is a specimen of magnetite-actinolite rock from the southeastern edge of the main bench of the American mine (Kelley, 1949, fig. 34). Quantita- tive spectrographic analysis of this sample by Janet D. Fletcher showed 0.008 percent BeQO. Sample 829-866¢ is a composite of fluorite ore (bastnaesite-bearing) from the Red Cloud mine. Quantitative spectrographic anal- ysis by J. K. Murata showed 0.0002 percent BeOQ. Dur- ing a previous mineralogical study of the bastnaesite (Glass and Smalley, 1945), spectrographic analysis had not detected any beryllium in this mineral (J. J. Glass, oral communication). The relatively high beryllium content of the sample from the American mine indi- cates that further sampling for beryllium in the district is warranted. LUNA COUNTY TRES HERMANAS DISTRICT The Tres Hermanas district is in the Tres Hermanas Mountains, just north of Columbus, in southern Luna County. Two localities in this district were visited on August 26, 1949. The geology of the Tres Hermanas Mountains was described briefly by Darton (1916, p. 79-82) and the mines by Lindgren, Graton, and Gordon (1910, p. 292- 295). The central mass of the mountains is composed of granite porphyry, flanked in part by andesite, rhyo- lite, and agglomerate, all of Tertiary age. In the north- ern part of the mountains some of the porphyry has intruded Gym limestone (Permian), which is up- turned and metamorphosed to garnet-wollastonite tac- tite. Spurrite has also been identified in the tactite (Lasky and Wooton, 1933, p. 83). 122 The principal mineral deposits are those at the north- western tip of the range which were mined for zinc. Limestone beds 1,000 to 2,000 feet north of the porphyry and limestone contact have been replaced by zinc and lead minerals. Most of the zinc is oxidized, principally to willemite; smithsonite, hydrozincite, and calamine are also present. A chip sample (329-756) of garnet- amphibole-calcite tactite from near the contact contains less than 0.0004 percent BeQO. The Tres Hermanas mine is at the contact of the por- phyry and the limestone on the east slope of South Peak. In this area the sediments have been metamor- phosed to interbedded garnet-tactite and calcite-marble for a distance of 150 feet from the contact. According to Darton (1916, p. 82), idocrase occurs at this locality. In a channel sample (329-760) taken of a 1-foot bed of the tactite, the BeQ content is less than 0.0004 per- cent. VICTORIO DISTRICT The Victorio district comprises a group of mines and prospects at the southeast end of the Victorio Moun- tains 3 miles south of Gage, a station on the Southern Pacific Railroad. The Victorio Mountains are a range of hills that rise about 800 feet above the neighboring bolson. The area was visited in September 1949 in the company of Mr. D. S. Tedford of Columbus, N. Mex., who generously supplied maps and information. Two days were spent in sampling and mapping an area con- taining beryllium-bearing veins and tactite deposits. Most of the production has been from the eastern part of the district, where mines in the vicinity of Mine Hill have produced more than a million dollars in gold, sil- ver, copper, lead, and zinc since 1880. In 1949, mining operations had ceased except for development work. The area containing tungsten and beryllium deposits is about a mile northwest of Mine Hill in sees. 29 and 30, T. 24 S., R. 12 W., New Mexico principal meridian. The deposits are mainly on claims of the Bogle group, including the Eloi, Morlock, Ogre, Bogle, and Yahoo claims, owned by D. S. Tedford, and the Tungsten Hill group, owned by H. R. Eaton of Silver City, N. Mex. Prospecting has been in progress for many years, and a little tungsten ore was produced in 1943. GEOLOGY Brief descriptions of the geology of the region are in reports by Lindgren, Graton, and Gordon (1910, p. 290-292), and Darton (1916, p. 83-85). The rocks of Paleozoic age are mainly limestone and include the Montoya (Ordovician), Fusselman (Silurian), and Gym (Permian) formations. These are overlain by Tertiary rocks consisting mainly of shales and sand- stones, with some coarse conglomerate beds. Thin flows OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES of andesite and rhyolite of Tertiary age form the top of the section. Most of the beds in the southern part of the range dip southward, but in the northern part they are flat or dip northward. Two or more thrust faults may be present in the region. In the area containing the tungsten and beryllium deposits, the Fusselman limestone does not crop out and may be absent as a result of faulting or of uncon- formable overlap. The Montoya and Gym limestones are cut by small masses of light-colored granitic rock. The mineral deposits occur mainly in veins and tac- tites in Montoya limestone. TUNGSTEN AND BERYLLIUM DEPOSITS Tungsten was first reported in 1908 from a vein on what are now the Eloi and Morlock claims (Hess, 1908, p. 726); the vein was described briefly by Lindgren (Lindgren, Graton, and Gordon, 1910, p. 292). Beryl was discovered in this vein in 1948 by W. P. Johnston of the New Jersey Zinc Exploration Co., Hanover, N. Mex. Helvite was found in the scheelite-bearing tactite de- posits east of the vein by W. I. Finch during the pres- ent investigation. The tungsten deposits are explored by several shafts and many prospect pits. The occur- rence of beryllium in the deposits has been discussed by Holser (1953). Samples obtain from the deposits are described in table 56 and the localities sampled are shown on figure 56.-Beryllia and tuzgsten in samples from the Victorio istrict [Spectrographic analyses by Janet D. Fletcher. BeO and W figures determined on gllatei exposed for general scanning but not for precise determination of BeO and W one BeO w Description (percent) - (percent) 6-ft channel sample of altered limestone from south end of pit on Bogle claim. Another sample reportedly from same gagity contained 1.06 percent Sample 329-390 0. 02 0. 02 SO: LVI rina iaa ases ania 392 4-ft channel sample of altered limestone from pit on Bogle Claim. clo ene eee a chau e oes ak 2-ft channel sample of altered limestone from pit on Bogle claim "nle cloe acto elk s Grab sample of serpentinized limestone with clay, from bottom of Bogle shaft._____.._. Grab sample of garnet marble from dump of Morlock shaft.. 5-ft channel sample of silicated limestone from collar of Yahoo : .s ce -a oe ao anes 4 . OX Grossularite - separated _ from sample 399-1. tl. 2007222082. 2-ft channel sample from lime- a stone on hanging wall of quartz vein near its north end, in prospect pit on Eloi claim_____ . 02 2-ft channel sample across quartz- muscovite-beryl-wolframite vein, same locality as sample 400 EAT ELLIE Ay . 08 . 0038 _ <. 01 393 . 004 _<. 01 394 . 005 _ <. 01 <. 001 . 06 397 399 399a 400 <. O1 401 LOCALITIES IN NEW MEXICO Taur 56.-Beryllia and tungsten in samples from the Victorio district-Continued BeO W Description (percent) _ (percent) 2-ft channel sample of limestone from footwall of quartz vein, same locality as sample 400 Chip sample from outcrop of 3-ft rhyolite dike, on Morlock IMMA 21 oo. oo see nee a o n+ mien mln t in Two 1-ft channel samples from quartz vein near its south end on Morlock claim__________... . 02 . 08 1-ft channel sample from quartz vein at bottom of inclined shaft on Morlock claim_________.__. . O1 R 6-ft channel sample of tactite from pit on Tungsten Hill No. $ : 1 cen lull eee eee sans s . 03 . OX Idocrase separate from idocrase- fluorite -tremolite-grossularite banded tactite, from pit on the Tungsten Hill No. 2 claim..._.. . 02 Grab sample of garnet marble and tactite, average of dump at shaft 2 on Tungsten Hill No. 3 AMM .c anne e ee eau taa a 4-ft channel sample of quartz vein from north end of 35-ft level, . O1 fI 4-ft channel sample of garnet tactite from western edge Eloi Claim". d . 06 . 06 Chip sample of 3-in. quartz- calcite-wolframite vein from shaft near middle of Eloi cece 2 e+ awh <= amon mls . 02 X Chip sample of fluorite-quartz fig), a few feet east of sample Chip sample of green clay-size material in altered limestone, from pit on Tungsten Hill No. P a Grab sample of garnet tactite from dump of shaft on Tung- sten Hill No. 2 Sample 402 0. 005 <0. 01 403 ©0083 : <.: Of 404 405 408 410a 411 ~. 006 . 04 414 415 416 417 . 005 - 2 418 . 008 - <. O1 420 002 -<. O1 85. Samples of the vein material contain as much as 0.2 percent BeQ and average about 0.04 percent; the maximum BeQ content of the tactite and marble sam- ples is 0.1 percent, with the average about 0.02 percent. These amounts are higher than those obtained in any other district sampled during the present investigation. Recovery of beryllium in connection with tungsten min- ing appears feasible, although the tonnage of tungsten ore probably is not large. Much of the beryllium in the tactite may not be recoverable and their tungsten content is low; the quartz veins are more promising. Quartz veins The main quartz vein strikes north for a distance of about 600 feet on the Eloi and Morlock claims, and dips 60° E. It is a uniform fissure filling from 1 to 2 feet thick, making sharp contact with the limestone. A shaft on the Morlock claim follows the vein down 85 feet to short drifts, above which small stopes extend upward. Several other shafts and pits have been dug along the vein outcrop. 128 Prismatic beryl crystals oriented perpendicular to the vein wall occur mostly as part of a selvage on the hanging-wall side. The beryl crystals, as much as 5 centimeters long and 1 centimeter in diameter, are bounded by simple prisms and pinacoid. The beryl is very pale green (5G 9/2) to colorless (Goddard and others, 1948). The refractive index (N,) is 1.574+ 0.001 corresponding to a composition of about 13.5 per- cent BeO. Milky quartz and some fine-grained musco- vite make up most of the vein. The tungsten mineral is a member of the wolframite series. Accessory min- erals are fluorite, galena, pyrite, wulfenite, lead car- bonates, and scheelite. The beryl-bearing selvage is most evident in the pits near the northern end of the vein. Beryl could not be seen in samples taken from the southern end of the vein and from the underground workings, but the analyses suggest that it is present. On the hill near the middle of the Eloi claim just below a conglomerate bed that presumably marks the base of the Gym limestone, several small veins have been prospected by shafts or pits (fig. 35). In the westernmost shaft, a 3-inch quartz vein contains calcite and wolframite, and a similar vein that crops out a few feet east is rich in fluorite. Samples 329-416 and 3829- 41" of these veins contained 0.02 percent and 0.005 per- cent BeQ, respectively. The walls of the main quartz vein are not greatly altered, the limestone retaining its gray color and fine grain; locally it contains small crystals of grossularite. Near the northern end of the vein, a sample (829-401) across the total width of the vein contained 0.2 percent BeO. A sample (329-400) across 2 feet of the hanging wall contained 0.02 percent BeO and a similar sample (329-402) of the footwall contained 0.005 percent BeQ. The small veins on the Eloi claim are bordered partly by tactite. Pyrometasomatic deposits Marble and tactite are most common on the Tungsten Hill No. 3 claim (fig. 35) where they occur as irregular lenses and bands several feet in length surrounded by unaltered Montoya limestone. The marble and tactite are not near an exposed intrusive body, although a small mass of granitic rock crops out on the hill to the north. Most of the altered limestone dip steeply. The most common type of tactite is a coarse aggre- gate of grossularite and calcite, although in some places the grossularite has entirely replaced the calcite. A pyroxene with optical properties near augite is a com- mon associate of the garnet. These minerals are re- placed by fine-grained tremolite and tale. A mineral resembling psilomelane coats some of the garnet. Scheelite is rare. Specimens of grossularite marble 124 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES MILES?! "DEming z'4 ON.) lb, , &i uh (s a Mine hill 2 Miles 329—4314 0.01 29—405 0 01 32-4030Q 329-404 002 EXPLANATION oreo Li > (Ro :]. (82 Faas g= Alluvium o Car /\ 4+ IEE ap- Il «g Granite & f § 65 C = / Gym limestone 5 Z / 329-410A 0. 2 I / 329—420 e g < < Gortat 117) @ Z £5 0 329-411; 0,006 Montoya limestone z a k /// (helvxte) TUNGSTEN HILL® 329-400 to 402; \/ 329—408 0. 03-d SHAFT # /i. Beryllla-bearlng tactite and marble Qall #s, ~ runesten Mu. én‘qdf $ Approximate contact 65 Strike and dip of beds 90 «ope Strike of vertical beds Horizontal beds f Qal A ‘_ cie if 5s . Quartz vein showing dip a Shaft X Prospect 329-394; 0.005 Locality sampled and number; A percent beryllia Nige © . Cal Base from claim map by D. S. Tedford G ~Geo-logy ‘by W. T. Holser and} o W. 1. Finch, September 1949 Figur® 35.-Tungsten and beryllium deposits in the Victorio district, Luna County, N. Mex. from the dump of the main shaft on the Tungsten Hill No. 3 claim, contained about 10 percent helvite. The helvite is medium yellow (5¥Y 7/6) (Goddard and others, 1948) very similar in color to several other min- erals in this district, such as grossularite, vanadinite- mimetite, and serpentine. However, the helvite is eas- ily recognized, for it occurs in distinctive sharp tetra- hedra scattered through the calcite. The crystals are about 5 millimeters across. Some are twinned on (111). The helvite has a refractive index of 1.73570.005, and a specific gravity of 3.25, corresponding to a composi- tion of about 85 percent helvite, 15 percent danalite (Glass, Jahns, and Stevens, 1944, p. 183). In thin see- tion the helvite is pale yellow, isotropic, and shows some dark peripheral zones of very fine inclusions, sim- ilar to the helvite from Casa La Plata, Cordova Province, Argentina, and Schwartzenberg, Germany (Fischer, 1925, p. 146). Crystals of grossularite are euhedral to subhedral against the helvite. A green tactite from the Tungsten Hill No. 2 claim is composed of bands of idocrase and fluorite alternat- ing with bands of tremolite, largely altered to talc, and garnet. The idocrase occurs as radiating clus- ters about 3 millimeters in diameter. It is anoma- lously biaxial negative, with a very small optic angle, and very low birefringence. The index of refraction (N. or N,) is 1.701+0.002. Spectrographic analysis of hand-picked grains (329-410A) showed 0.2 percent BeO. In the southern part of the area, on the Ogre, Bogle, Morlock, and Yahoo claims, exposures are poor. Pits expose several feet of loose bouldery material partly cemented by caliche. The lower part of the loose mate- rial is nearly in place, apparently a product of weather- ing from the underlying pediment. The rock is highly oxidized and appears to have been originally marble containing garnet and pyroxene. Specimens from shafts on the Ogre and Bogle claims were particularly rich in serpentine. A sample taken from one of these prospects by the U. S. Bureau of Mines was reported to contain 1.06 percent BeO (J. H. Soulé, 1949, personal communication). The highest value obtained in sam- ples of altered limestone and marble taken during the present examination was 0.1 percent BeO (see table 56, samples 329-890 to 329-399). Helvite was seen only in the specimens from the shaft LOCALITIES IN NEW MEXICO on the Tungsten No. 3 claim. To trace the occurrence of beryllium in the other tactite, several samples whose analyses showed beryllium were separated in heavy liquid. The heavy separate (mostly grossularite) was tested for helvite by staining (Gruner, 1944), and the light separate (mostly carbonates) was examined opti- cally for beryl. In several thousand grains examined, no grain of either mineral was found. Idocrase was found in only one sample (829-410). Grossularite was separated from a sample containing 0.1 percent BeO (329-399), but was found to contain only 0.007 percent BeQ. The mode of occurrence of beryllium in the tactite may be similar to that in the tactite at Iron Mountain, N. Mex., where beryllium occurs in several silicates and an unidentified alteration product (Jahns, 1944b, p. 58). oTERO COUNTY The occurrence of beryllium in the feldspathoidal igneous rocks of the Cornudas Mountains, southern Otero County, is discussed in the section on the Trans- Pecos Region, Texas and New Mexico. The mines of the Juarilla district, northwest of Oro- grande, expose extensive tactite zones (Lindgren, Gra- ton, and Gordon, 1910, p. 184-187). Earlier sampling of some of this tactite by the American Smelting and Refining Co. did not detect any beryllium. The district was not visited during the present investigation. SAN MIGUEL COUNTY ROCIADA DISTRICT The Rociada district is in the eastern foothills of the Sangre de Cristo Range. It is reached by improved roads leading westward from State Highway 3. The district was visited on July 20, 1949. The geology of the district was described briefly by Harley (1940, p. 52-56). The mineral deposits are in Precambrian gneisses and mica schists that have been intruded by sills of diabase and masses of granite. Quartz veins in the metamorphic rocks contain pyrite, chalcopyrite, bornite, chalcocite, sphalerite, and galena, with minor amounts of gold and molybdenite. At the Azure-Rising Sun mine, 4 miles southwest of Rociada, tactite minerals are associated with the veins in quartz-biotite schist. Epidote, garnet, amphibole, specularite, and tourmaline occur in the ore and in ad- jacent wall rock. A grab sample (329-384) from the dumps containing both ore and wall rock contains less than 0.0004 percent BeQ. WILLOW CREEK DISTRICT The Willow Creek district is on State Highway 83, about 14 miles north of Pecos. The Pecos mine, which 125 has been one of New Mexico's principal metal produc- ers, was visited on July 21, 1949. The geology of the mine is discussed in many papers, which are summarized and supplemented by Harley (1940, p. 69-89). The mineral deposits are in Precam- brian schist and diabase intruded by Precambrian granite. These rocks are exposed in a window in lime- stone of the Magdalena group (Pennsylvanian and Permian). The ore deposits occur along a shear zone that trends northeasterly through the schist and di- abase. The ore contains pyrite, sphalerite, chalcopyrite, galena, pyrrhotite, bornite, and gold. Chlorite, actino- lite, sericite, quartz, tourmaline, and roscoelite have formed in the wallrock. A grab sample (329-386) of ore and wall rock from the main dumps at the Pecos mine contains less than 0.0004 percent BeQ. SsANDOVAL COUNTY COCHITI DISTRICT The Cochiti, or Bland, district is in the Valles Moun- tains about 30 miles west of Santa Fe. The geology of the district was described in detail by Graton (Lind- gren, Graton, and Gordon, 1910, p. 150-162). Intru- sive monzonitic rocks that are exposed in the lower parts of the canyons are covered by extensive flows of rhyolite. Quartz, sphalerite, pyrite, and chalcopyrite with minor amounts of argentite and gold, were de- posited along fracture and breccia zones in the mon- zonitic rocks. According to Mr. C. W. Arnold of Pena Blanca, N. Mex. (personal communication), a vein at the Big Sambo mine, near Bland, was reported to contain as much as 1.0 percent BeQ. The mine workings consist of a short adit in monzonite and a crosscut that inter- sects a fracture zone containing quartz and calcite. The monzonite is highly altered. Two samples were taken at the mine by J. W. Adams of the U. S. Geo- logical Survey. A 6-foot channel sample (JA-49-4) across the fracture zone contained 0.0005 percent BeO, and a grab sample (JA-49-5) of the altered monzonite contained 0.0007 percent BeQ. SANTA FE COUNTY NEW PLACERS DISTRICT The New Placers, or San Pedro, district is in south- western Santa Fe County, just east of the village of Golden on State Highway 10. It was visited on July 12 and 13, 1949, when, except for the New Placers mine on the northern slope of the mountains, the district was inactive. 126 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES EXPLANATION Qal Alluvium Limestone and sandstone Mostly limestone of Pennsylvanian age in the San Pedro Mountains; mostly sandstone of Cretaceous age in the Ortiz Mountains. - Locally metamorphosed to tactife or hornfels J J\ / PENNSYLVANIAN AND _ QUATERNARY -v CRETACEOUS v TERTIARY Intrusive igneous rocks Mostly syenite; some diorite, some rhyolite porphyry sills Contact mS Mine +3 Locality sampled 35° 19 =a o "B J °10 Geology compiled by W. T. Holser from unpublished maps by J, F. Smith, Jr., and A. H. Wadsworth, Jr., U. S. Geological Survey (San Pedro Mountains) and by C. T. Griswold, Ortiz Land Grant Co. (Ortiz Mountains) FrGurE 36.-Geologic map of the New Placers and part of the Old Placers districts, Santa Fe County, N. Mex. Base from U. S. Soil Conservation 10 Service planimetric map 1 0 1 Mile je 1 1 1 1 1 LOCALITIES IN NEW MEXICO The geology of the district was described by Yung and McCaffery (1903) and by Lindgren (Lindgren, Graton, and Gordon, 1910, p. 170-174). The major geologic features are shown in figure 36. The sedi- mentary rocks in the San Pedro Mountains consist of about 1,500 feet of flat-lying limestones, shales, and sandstones of the Madera formation (Pennsylvanian) In the western part of the mountains is a laccolithic mass of porphyritic rock that appears to be mainly syenite and monzonite. Two 60-foot sills that are strati- graphically above and below the laccolith are of younger rhyolite porphyry. The small intrusive bodies in the eastern part of the mountains are diorite. Near the laccolith and beneath the upper rhyolite sill, shale is altered to hornfels and limestone to tactite. Garnet is the most common mineral in the tactite, but diopside, feldspar, quartz, specularite, epidote, ido- crase, and wollastonite are also present. Some of the limestone has been changed to coarse white marble. The ore deposits are in the metamorphosed rocks be- tween the laccolith and the upper rhyolite sill. The chief ore mineral is chalcopyrite. It is disseminated, along with some scheelite and molybdenite, in the tac- tite and marble. Samples were taken at most of the mines in the dis- trict, as shown in figure 36. The samples are described in table 57. TaBu® 57.-Beryllia in samples from the New Placers district [Spectrographic analyses by Janet D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] 127 Tasus 57.-Beryllia in sarrggles from the New Placers district- ntinued BeO Sample Description (percent) 336 Grab sample of garnet-epidote tactite at face of New Placers adit._______------ <0. 0004 340 Grab sample of 1-ft quartz vein and asso- ciated quartz-garnet tactite of the "50 beds"(?), near Montezuma shaft__.-.. <. 0004 341 - 15-ft channel sample of garnet tactite with copper stains, from the "50 beds" at Vir- ginis <. 0004 342 6-ft channel sample of garnet tactite with chalcopyrite, from "24 beds" at Virginia sz _. cu nant oo - bn ans sm <. 0004 345 Chip sample from outcrop of syenite near its upper contact with Madera forma- tion, west of the Montezuma shaft___. . 0004 OLD PLACERS DISTRICT The Old Placers district, also known as the Dolores or Ortiz district, is in the Ortiz Mountains just north of the New Placers district. It is east of State High- way 10 and is accessible by several unimproved roads (fig. 36). The district was visited on July 13, 1949. The geology of the region has been briefly described by Yung and McCaffery (1903) and by Lindgren (Lind- gren, Graton, and Gordon, 1910, p. 167-170). Mr. Griswold of Albuquerque, N. Mex., who has worked in the district for several years, furnished further infor- mation on the geology of the Ortiz Mountains. Sedimentary rocks, mainly the Mancos shale of Cre- taceous age, are invaded by intrusive igneous bodies which, according to Griswold, are thick sills, Most of the igneous rocks are granular and composed of horn- blende and andesine, but the composition varies con- : BeO siderably ; some are porphyritic. These rocks were called Sample Description (percent) y 329-323 6-ft chagilel samOpLe g’f, verlérI coarse mall'ble ' syenite porphyry by Yung and McCaffery (1903, p. from "lower 50 bed" in Home tunnel.. . 0004 H lori F m ili 324 - 6-ft channel sample of garnet tactite, with 851), essexite, diorite, dacite, and ajndesflte by pgflwe alkalcfipg'ite, frgn} Swan tunnel at west stool (1908, p. 230), and quartz monzonite, monzonite, and side Richman t A Ant A 325 6-ft channel sample in garnet-calcite tac. diorite by Lindgren, .Grraton, and Gr'ordon (1910, p. 40). tite, with chalcopyrite, from Swan tunnel <. doo4 Near the Black Prince (Old Reliable) and Pat Col- das ® ; a s 326 (Hg channel sampli of garnet tactite from ~ looek lins claims (fig. 36) along Alpine Gulch, most of the wan tunnel workings. _________-__---- y 898. | Sift channel sample of garnet:onleite from Mancos- slfale has been metamorphosed to hornfels, ax-ld Swan tunnel workings. _____-___-_---- <. 0004 | locally it is completely altered to a coarse garnet tactite 333 4-ft channel sample of garnet tactite re- fios h s > ] £ placed by copper, iron, and manganese containing chalcopyrite, pyrite, and go d. Tactite oc- $523???) har ons (?), upper part of «. 0004 | CUS also in the next canyon north and on the Buckeye 334 Chi? saéngle of 1.5 ft of garngt tactite re- claim to the northeast. No tactite is present at the Can- placed by copper, iron, and manganese ABH § minerals, lower part of Spanish opencut. - <. 0004 delaria mine, the largest in the area. FiGurE 36-Continued MINES AND LOCALITIES SAMPLED 1. Buckeye 7. New Placers adit 329-336 12. Home tunnel 829-323 2. 329-350 8. 329-345 13. Richman shaft 3. 329-349 9. Virginia adit 329-341 and -342 14. Swan tunnel 4. Black Prince 10. Montezuma shaft 329-340 329-324 to -326, -328 (Old Reliable) 329-353 11. Spanish opencut 15. Carnahan 5. Pat Collins 320-333 and -334 16. Lazarus 6. Candelaria 128 Samples of the igneous rocks and tactite that were analyzed are described below; localities sampled are shown on figure 36. Bample Description 820-349 Specimen of leucocratic pyroxene syenite(?) from locality 8. 850 Specimen of syenite(?) from main intrusive body at locality 2. 853 6-ft channel sample of garnet tactite from opencuts on Black Prince claim. 359 Specimen of porphyritic intrusive rock from road cut where State Highway 10 turns northeast across Ortiz Mountains (not shown on fig. 36). These samples do not contain as much as 0.0004 per- cent BeQO. SIERRA COUNTY APACHE NO. 1 DISTRICT The Apache No. 1 (Chloride) district is on the east slope of the Black Range, a few miles southwest of the old mining camp of Chloride (fig. 37). Production amounting to less than a million dollars has been £27. " Chip 5 f Veride *n ___, # e I? Creek _ Chioride sory 33°20 . e Z 5. rheasumy mine *3 \ - * sr. coup mine traa;f\f$§ é?“ * mromeont jet pa mime m m BALD EAGLE MINE & ay yongment Mowe zA oM a a- nenmoSh a mies I 0 107°40 ARG \fifif’.‘._\_fl S899 37.-Index map of the Apache mining district, Sierra County, N, Mex. mainly in gold, silver, and copper. The district was visited on August 21 and 22, 1949, and there was little mining activity at that time. The geology and mineral deposits of the area have been described by Harley (1934, p. 73-77) and by Gor- OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES don (Lindgren, Graton, and Gordon, 1910, p. 260-266). The sedimentary rocks are limestone of the Magdalena group (Pennsylvanian) and Abo sandstone (Permian), which dip eastward on the lower slopes of the range. They are overlain on the upper slopes by Tertiary vol- canic rocks, including andesite, rhyolite tuff, and brec- cia. No intrusive rocks are exposed in the district, the nearest being a large monzonite sill in the Cuchillo Negro Range several miles east of Winston. North- trending normal faults slice the eastern part of the range into long narrow blocks that are downthrown on the east ; cross faulting is common. Most of the veins are fissure fillings in andesite, but some are traceable into underlying limestone. The principal metallic minerals are pyrite and chalcopyrite, with associated gold and silver. The gangue minerals are quartz and calcite, with some barite. The veins show delicate banding and crustification. Harley (1934, p. 76) classified the deposits as epithermal. Samples were taken only at the Midnight mine, where small amounts of garnet and epidote had been reported (Harley, 1934, p. 85). The vein is principally quartz with some calcite and fine-grained epidote. Limestone on the footwall is marmorized and silicified ; greenish sandstone forms the hanging wall. Ore on the dump contains bornite and copper carbonates. A sample (329-705) cut across the vein at the collar of the south shaft contains less than 0.0004 percent BeO, but a grab sample (329-706) of copper-rich ore from the dump contained 0.01 percent BeQ. Further sam- pling is needed to determine the nature and extent of the beryllium-bearing material, CUCKHILLO NEGRO DISTRICT The Cuchillo Negro district, which is south of State Highway 52 in the Cuchillo Negro Mountains, was visited on August 21, 1949. The geology, as described by Harley (1934, p. 113-125), is similar to that in the Apache district a short distance west in that an east- wardly dipping section of about 1,500 feet of limestone of the Magdalena group (Pennsylvanian) is overlain by Tertiary volcanic rocks. A thick sill of monzonite porphyry about 8 miles long intrudes the limestone, which has been replaced along fractures by garnet, epidote, and quartz, accompanied by galena, sphalerite, chalcopyrite, and oxidation products. Samples were taken in the vicinity of the Sentinel (Dictator) mine, which is reached by a road turning south from State Highway 52, about 2 miles west of the HOK ranch. The mine is described in detail by Harley (1984, p. 120-123). A grab sample (329-700) of galena-sphalerite-calcite ore from the dump of the Sentinel adit contained 0.001 percent BeQ.. Sample LOCALITIES IN NEW MEXICO 329-701 from the same dump was composed of garnet, epidote, quartz, and calcite, and contained 0.0007 per- cent BeQO. 'A sample (329-702) of highly altered rock from the monzonite next to its contact with the marble at the Sentinel shaft contained 0.0005 percent BeQ. The area to the north and west of the Sentinel mine, including the Silver Bell mine, was also inspected, but no other tactite bodies of any consequence were found. Although the geology of this district is somewhat similar to that at Iron Mountain immediately to the north, the ore bodies are small and the beryllium con- tent of the tactite is apparently low. IRON MOUNTAIN DISTRICT Pyrometasomatic deposits containing beryllium and tungsten occur in an area of about 15 square miles, largely in northern Sierra County but extending into southern Socorro County. The deposits were studied and sampled in detail by the U. S. Geological Survey and the U. S. Bureau of Mines during 1942-43 (Jahns, 1944a, 1944b; Glass, Jahns, and Stevens, 1944; Storms, 1947). The district was visited briefly on August 22, 1949, in connection with the present investigation. Little development work had been done since 1943, and further sampling was regarded as unnecessary. Tron Mountain is a narrow north-trending fault block composed mainly of eastward-dipping rocks of late Paleozoic age of the Magdalena group and Abo sand- stone. To the east, these rocks are overlain by Cretace- ous sedimentary rocks which are in turn overlain by several thousand feet of Tertiary volcanic rocks,. Sills, dikes, and pluglike bodies of monzonite, rhyolite, gran- ite, and aplite cut the sedimentary rocks and part of the volcanic series. The sedimentary rocks in the Iron Mountain block were contact-metamorphosed next to the intrusive bodies, and some of the more calcareous rocks were altered to tactite, particularly at the north- ern end of the block. Two main types of tactite are recognized: a massive, garnet-rich tactite and a banded tactite, or "ribbon rock." The massive tactite is locally rich in magnetite or fluorite, and parts of it contain sufficient scheelite and powellite to be valuable as tungsten ore. The "rib- bon rock" consists mainly of magnetite, hematite, and fluorite, with some garnet, diopside, idocrase, and other silicates. It contains virtually all of the beryllium, mainly in helvite but some in grossularite, idocrase, chlorite, and other minerals. Beryllium reserves of the district amount to 3,500 tons of indicated ore and 1,000 tons of inferred ore, both containing an average of 0.7 percent BeQO, and 84,000 tons of indicated ore and 100,000 tons of inferred ore thought to average about 0.2 percent BeO (Jahns, 467945-59--10 129 1944a, p. 76). Recovery of the beryllium involves rather complex mining and metallurgical problems, and there has been no production. Results of flotation ex- periments conducted by the U. S. Bureau of Mines on similar ores (Kennedy and O'Meara, 1948) suggest that ultimately the problems may be surmounted. socoRrRO COUNTY JONES CAMP DISTRICT Jones Camp is on Chupadera Mesa in eastern Socorro County, north of U. S. Highway 380. The area was not visited, but a specimen of tactite from one of the deposits was obtained from V. C. Kelley. The geology of the district has been described in de- tail by Kelley (1949, p. 213-222). Chupadera Mesa is capped by sandstone, limestone, and gypsum beds of the San Andres and Yeso formations of Permian age. An anticline in these rocks is intruded by a dike that trends northwest along the fold axis for about 10 miles. The dike is complex, consisting mainly of mon- zonite and syenite, with some later but closely asso- ciated diabase. A narrow and irregular metamorphic zone composed of actinolite, tremolite, and magnetite occurs in the sedimentary rock along the dike. The magnetite ore bodies replace actinolite rock, diabase, and limestone. A. specimen (sample 329-809) of actinolite tactite from the contact of the diabase dike in trench 9 (Kelley, 1949, fig. 44) contains less than 0.0004 percent BeQ. TAOS COUNTY RED RIVER DISTRICT The Red River district is on the western slope of the Sangre de Cristo Mountains and is crossed by State Highway 38. The district was visited on August 80- September 1, 1948. E. C. Anderson and P. F. McKin- lay of the New Mexico Bureau of Mines, who accom- panied the party, suggested areas for sampling. The geology of the district was described briefly by Graton (Lindgren, Graton, and Gordon, 1910, p. 84- 88) and the Questa mine was described by Larsen and Ross (1920) and by Vanderwilt (1938). More recent work by the New Mexico Bureau of Mines and the TU. S. Geological Survey (Park and McKinlay, 19482, 1948b) deals only with the part of the district south- east of the area sampled. The Precambrian rocks of the district include horn- blende gneiss, schists, and quartzite that are intruded and locally replaced by granite. Conglomerates, shales, limestone, and sandstones belong at least in part to the Magdalena group of Pennsylvanian and Permian age. These rocks are intruded by stocks and sills that range in composition from granodiorite and monzonite to 130 granite. Later intrusions and flows of andesite and rhyolite cover much of the area. The structure is com- plex. In general, hydrothermal alteration has been intense in the district, particularly in the granodiorite west of Red River. At this locality quartz-gold veins occur both in the granodiorite and in overlying volcanic rocks. In places along the granodiorite contact, as at the Hornet mine on Cabresto Creek, some galena and sphalerite occur with garnet and other tactite minerals. The Questa mine is near the edge of a small granite stock and explores quartz veins containing molybdenite, fluorite, pyrite, and rhodochrosite. The granite and sedimentary rocks nearby are almost entirely altered to chlorite and clay in the vicinity of the mine. Most of the sampling was confined to the molyb- denum-rich area between Red River and Questa; the samples are described in table 58. The analytical re- sults indicate that the molybdenum-bearing veins and altered granitic rocks contain small quantities of beryl- lium, though probably not enough to be recoverable by present methods. in samples from the Red River district [Quantitative spectrographic analyses by A. A. Chodos] BeO Sample (percent) 829-214 Description Grab sample along 6 ft of outcrop of 6-in. fluorite vein in rhyolite, Chokecherry Canyon, 3 miles east of Questa_._______ Grab sample of highly altered monzonite on the north side of Red River Canyon, 3 miles west of Red River_____________ Grab sample of yellow clay from same alteration zone as sample 221. Sample of heads from molybdenum ore run August 31, 1948, Questa mill_ _ ___ Specimen of rich molybdenum ore from Questa mine co 5 l uds oh c_ 4-ft core of tailings pile at Questa mill___._ Specimen of alaskite, with molybdenite veinlets, from dump of Questa mine___. Specimen of coarse granitic rock, with molybdenite veinlets, from dump of Quesb® MIMIC .n. L co ae al 2 need wee 2 e ae nl nel 4-ft channel sample of molybdenite vein, 200 ft inside north tunnel of BJB mine, 314 miles east of Questa__________..__. f Grab sample of garnet-rich galena-sphal- erite ore from dump of Hornet mine, north side of Cabresto Creek 7 miles East OL LZ . onne ec sink ns Channel sample across 10-ft vein of quartz, calcite, pyrite, and galena, between granodiorite and quartzite, at upper tunnel of Hornet mine_______________. 0. 0007 221 <. 0003 <. 0003 . 002 . O01 . 004 . O01 222 223 226 227 233 234 . 0005 236 . 0005 237 . 0008 238 . 0003 TRANS-PECOS REGION, TEXAS AND NEW MEXICO By W. T. Houser INTRODUCTION The study of beryllium-bearing rocks in the Trans- Pecos Region was restricted to the relatively flat and barren Diablo Plateau in Hudspeth, Culberson, and El Paso Counties, Tex., and Otero County, N. Mex. This OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES plateau is at an altitude of 3,500 to 5,000 feet and is bounded on the west and south by Rio Grande valley, on the east by Salt Basin, and on the north by the Sac- ramento Mountains. The edges of the plateau are char- acterized by a rough scarp topography resulting from headward erosion of tributary streams into flat-lying sedimentary rocks. Laccoliths, plugs, dikes, and sills of more resistant igneous rock form erosion remnants that are prominent features of the landscape. Early reconnaissance surveys by Baker (1927), Beede (1918), and Richardson (1904, 1909, 1914), and recent work by King and others (King, 1948, 1949) ; King, Branson and others (1949); King, King, and Knight (1945) ; King and Knight (1944) ; Adams and others (1949); and Smith and Albritton (1949) em- phasized the sedimentary rocks and their structure. Huffington (1943) described in detail the igneous rocks of the Quitman Mountains and Clabaugh ', Timm ®, and Zapp ® made detailed studies of the igneous rocks of the Cornudas Mountains. Most of the Diablo Plateau is underlain by flat-lying limestone of Permian age that unconformably overlies older Paleozoic and Precambrian rocks. These rocks are exposed only along the eastern margin of the plateau where they have been upthrown by faulting and folding. Cretaceous and Jurassic sedimentary rocks crop out in the southwestern part of the plateau and are complexly folded and faulted. The sedimentary rocks were intruded by laccoliths, plugs, sills, and dikes of alkalic igneous rocks, probably of early Tertiary age. In most places, contact metamorphism and metaso- matism have been slight, although rather extensive zones of marble, hornfels, or tactite were formed around a few of the intrusive bodies. Samples of igneous and contact-metamorphosed rocks collected during an earlier trace elements investi- gation by the U. S. Geological Survey from Cave Peak, Culberson County, Tex., and Wind Mountain, Otero County, N. Mex., were reported to contain as much as 0.3 percent BeQ. The igneous rocks of the Trans-Pecos Region were known to include feldspathoidal types that, on theoretical grounds, are likely to contain beryl- lium-bearing minerals. The region was, therefore, marked for special study during the present investiga- tion. During August 1948, the Cave Peak and Wind Moun- tain areas were studied and resampled by Holser and Wilmarth. Detailed geologic maps were made of the beryllium-bearing localities in these areas by Holser and 7 Clabaugh, S. E., 1941, Geology of the northwestern Cornudas Moun- tains, N. Mex. : Univ. Texas M. Sc. thesis. ® Timm, B. C., 1941, Geology of the southern Cornudas Mountains, Texas and New Mexico: Univ. Texas M. Sc. thesis. * Zapp, A. D., 1941, Geology of the northeastern Cornudas Mountains, N. Mex.: Univ. Texas M. Sc. thesis. LOCALITIES IN TRANS-PECOS REGION W. I. Finch in July 1949. A general reconnaissance was made of the other intrusive igneous rocks in the region. P. B. King, Earl Ingerson, Charles Milton, and J. F. Smith of the U. S. Geological Survey supplied the field party with information about several of the areas visited. INTRUSIVE IGNEOUS BODIES AND CONTACT ZONES Most of the intrusive igneous bodies of the Diablo Plateau are small, ranging from laccolithic masses as much as 3 miles in diameter, and sills as much as 1,500 feet thick, to dikes less than a foot thick. The majority of the rocks are alkalic; most are silica-rich, but many are feldspathoidal.. With few exceptions they are suf- ficiently similar in composition to suggest that they represent a petrographic province. The highly de- formed Quitman Mountains are included in the Trans- Pecos Region for convenience although their struc- tural setting and granitic rocks are more nearly com- parable with the mountains of the Arizona and New Mexico region. They contain some syenitic rocks which are common in the Trans-Pecos but unknown in the Arizona and New Mexico region. The areal extent of the intrusive igneous rocks in the Trans-Pecos Region is shown in plate 1. The general distribution is peripheral to the Diablo Plateau. Most of the intrusive bodies were examined, and many sam- ples of the igneous and associated metamorphic rocks were taken. Brief descriptions of the bodies, the con- tact zones, and the samples collected are given, together with analytical data, in table 59. Little beryllium is indicated in these rocks, except at Wind Mountain and Cave Peak. SYENITIC ROCKS Syenites are common in the region, particularly in the northern part (table 62). The most characteristic rock is a fine-grained, dark gray-green syenite contain- ing small phenocrysts of feldspar. Its principal min- erals are sodic plagioclase and sodic pyroxene; the pyroxene ranges in composition from aegirite to augite. Potassic feldspar, sodic amphibole, and biotite are less abundant. Many of the syenites contain small subhedral crystals of analcite or nepheline in the groundmass. Several of these intrusive rocks, such as those at Alamo Mountain, Sierra Tinaja Pinta, and Sierra Prieta, have a finer grained, dark schistose bor- - der phase just above the basal contact. The structure parallels the contact in most places and is the result of orientation of the dark minerals by flow. A less common coarse-grained and porphyritic sye- nite forms the main intrusive masses of the Wind Moun- tain, Little Wind Mountain, and Black Mountains. 131 Phenocrysts of perthitic feldspar, as much as 1 inch long, constitute most of the rock. Smaller crystals of perthitic feldspar, nepheline, analcite, aegirite, and minor amounts of biotite form the groundmass. Both the large and small perthitic feldspar crystals show a pronounced orientation caused by flow. The border phase of this rock is darker, finer grained, and nonpor- phyritic. Similar porphyritic syenites form the intru- sive bodies at Cornuda Mountain, Granite Mountain, and Hueco Tanks. The norm of these rocks contains no nepheline, and none was seen in thin section. The coarse-grained syenite of Marble Canyon in the Sierra Diablo, according to Charlee Milton (1941, written communication), contains more than 50 percent sodic plagioclase that is intergrown perthitically with some potassium feldspar. Highly altered hornblende and biotite are the only mafic minerals. About 6 per- cent quartz is graphically intergrown with the feldspar. The boarder phase of this syenite is a finer grained mela-syenite. Subsidiary intrusive bodies are remarkably lacking around and in most of the large syenite masses. Most of the intrusive bodies are single masses of rock that have sharp boundaries with the surrounding sediments. The intrusive mass at Marble Canyon, however, has a number of associated aplite dikes and one nepheline syenite dike. The main intrusive mass at Wind Moun- tain is surrounded by numerous small dikes and sills, most of which are medium-grained, dark aegirite- nepheline rocks (malignite); some are feldspar-rich and are coarse grained or pegmatitic in texture. The only other dike rocks seen along the many miles of igneous contact examined were a few thin phonolite dikes at the southern contact of the intrusive body at Sierra Prieta. It may be significant that the dike rocks apparently are associated only with the coarse-grained porphyritic syenite intrusive rocks. GRANITIC ROCKS Granitic rocks are found in the intrusive masses in the Quitman Mountains, Wylie Mountains, Sierra Blanca, Cave Peak, and Sierra Diablo. Most of the Quitman Mountains mass is a medium-grained quartz monzonite that contains orthoclase, oligo- clase, biotite, and small grains of quartz. Gran- ite occurs in the southwestern part of the intru- sive mass (Huffington, 1943, p. 1035) and locally rocks are syenitic. - Small diorite xenoliths are present in the quartz monzonite. In the Wylie Mountains and at Sierra Diablo the granitic rocks occur next to intrusive syenitic rocks. The central part of the intrusive mass at Cave Peak is composed of granite, associated with rhyolite porphyries and breccias. 132 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES auo N *19%1U09 WI9]89M -Yj10U WoIJ o[Gietu pus P00 '> _ suoxor{d jo usaurpadg - g1g ews Jo qs auojsowl[ pus FO0 >> -uo; jo ordwres jouueyo 3;-g - 960 WojsoM Wo Aikudaod poiope F00 *> _ 4tq®tq go ordures jouurego 1p-g - 960-628 guo N quo n quo *opts tio -jsam wo; oyuo4s ouro 9900 * -ydou amm4ydaod ;o uowradg - pgg WIojs9MuJNOS WoJJ oqruods ommu4udrod pais; ©00 © -Is Jo jouueyo 3g - 609 *sSEUI UIBUI JO 911 $000 © -uo4s ;o uowroadg - 19-628 Cie A aaa art a *opts wo; ojyuo4{s _ outfoudou ©00 oq10reut remueid ;o usawroadg - ga9-6Z2 guo guo N *opts wor; £00 © oqruods jo uswadg - gqg oy} Jo opts qstoyjiou wo; Li4ydaod 100 '0 _ oqtuods omorq ;o uowadg - 1099-6Z8 guo N 038.65. uoyduoseq “MN 0°g sordung ||||||||||||||| guo N '°1q -IBUW JO JUOZ MOLIBU 04 auo3spureg 'uon sag -Is pus arqreur soupy ....... poaosqo auo ||||||||||||||| N '211108} puse oqieu cout auoxoI£4q4 ||||||| auo N ...... uo €orfIs 1ourpy ||||||||||||||| quo N wsrydiowngap; 'yqnos Uf auo4s2w1] Sundg ouog ur ouojsow!f osonpg *puo uo 18 ouojsou| ooong, {(;) dnous Jo ouojspueg Sundg ouog '() dnous Jo *pasod -xo jou'dnos €11qSE M *dnous Jo *pasod -xo jou 'dnous e1rqsSeMA *dno18 Jo ouo:spusg ...... auojsowf[ 'oreys popnfout Y}IMA ouo;sout ojonpg; ........ posodxa auo Surrdg auog *dnous Jo auojs -owl[ pues ...... auojsout p( uuuuuuuuuuuuu op----- ........ posodxa auopy 1 4004 papnguy *puo 1100 48 oxIp qaog®e 1osreo9 'Arkyd -1o0d oyyuo4s Jo IIIS '1opdoq poute13-ou1; 'Ai4yudaod oqruods as1eo9 JO IIIS 33-009 'x214} 3; 03 dn oytuads ;o s[[Ig *Aikqdaod ourroydou Jo yj!J0098]| 18] -o4s ojtoreue Jo 1[!S 1J-00F -o4s oytoreue Jo 1109987 'opruads ourfoydou onudqdrod ;o IIIS 3J-00Z 'oqruods onuXAqdrod ;o (;)4}1109987 *orqerrea soseqyd aytp pus Iopdoq {oqrua4ds ourfroudou onufudiod ;o - '1opao; qsomuqnos JIM 'optuo4s -use Jo *opIs qstoyoU 16 oxIp opuo{s ouSne fKikyudaod our -oydou ;o IIIs 1J ¢2-03-08 'omukyd -10d auros 'aqrfouoyd ~org-ourrogdou ;o IIS 13-008 ................. op----~ '&akqd -10d aytuo4s ogrorq Jo SuId -10d aqyuads jyo 3004 snoau0; uorbar; soo2 ay; fo qind fo sauoz joofu0a pun syoou ur nyhuog-6gq s794v 1, ........... 0898 3e9d4 ..... urequnojy 49[[I VIINIGd YIVNLL YHHZIS ...... surequnopyt Sog ~urequnopt uingyseM 'ureq -unopy oruojuy usg ..... sepnuio; ...... urequnopy *(urequnopy 499) PUM ~~~-urequnopy doj}¥q ~~~~-ure;unopy osy SNIVLNAON SYINANHOD |||||||||| OLI19() ........ ooonp; ........... 9018 894 SNIVILNNONK OoAUH ___ pauy 8T PI 8T ZI If Ot 138) LOCALITIES IN TRANS-PECOS REGION £00 *> $00 *> £00 *> 100 *> 's9 o1qe} 998 ('Afoyexe -dos por{reus youg) ©1398} -Uod WoJJ $390Uu8} -stp Surérea 346 ofqrew pus ;o sordures jfouursyo 2 'IIIs [Tews 1e oreqs pasoyye ut ardures fouurego 1}-z q89MuJNOS orqrew ut ordures fouureyo 3J-p *opts y3nos uo L14ydaod auon auon auon auon auon auon guo n auony 820 6T PII-628 auon auon ur oyip jo uownoodyg #p60-668 "(éret) uomuary pus '(6r61) szoqgo pus 'uosuerqg '3urst '(6p61) pus surepy 99s 'stresop oryde13y21}8 10, ; .............. 8-5 .............. $p... .............. opr > .............. ip.. .............. op- ~~~ ....... suo op ~- ....... paa1asqo uo ~ UoI}EZIIOULIEBUI JOUIJA *sotoe; ajturptues Jo stoJu1oy, pus arqiswu 3} 00F 0% 0 *soroe; Jo s[oJU1O4 puse ofqieur Jo 1J (OF 'Uor} -eols outmu 'ou038s -owu1 pozffeqs410991 puse poyosolq 1J 0G-€ ............ oqrzqrent 1 qq ouos orqiew ews 0%4u09 48 quo *arqrewu fourzqrenb yrep 0; quojspusg *dno18 Jo ouojspUeg *dnous Jo 9uojsoWI| *dnous Aqtuuy Jo .............. op---~ Jo ouo;souf| *dno1s 3ingsyot -13por{ Jo ouojsputeg *dnous Equi; Jo 91819 -Wwo[3u00 pus 9u0}8 'soti9s p1BU09T ;o puse 'oreys *dnous -10por{ Jo ouojspueg ...... auojsowt[ OJnp |||||| auojsowff OJon | _ *squo4s9u1] Suudg ouog pus f; *dno18 -pol{ Jo ouojspuss o; ouojsowl OJonpg *auo;spues dnois SingsyoLl9poIA ~auo4sou1 Suridg auog *y,I0U ur auojsowuf[ OJonp yinos o; (;)dnois €iigseM uf ouogspueg oyjofy1 ;o ss pus SoYI( .................. op- ~~~ .................. op-~-~ .................. op---- *() H -ue13s oyrgnt Jo Yj0998T '&akqd -10d JO SIIG *Aikqd4od apuotq -u1oy Jo soxIP 1J-001L 0% OT 'o,1u04s opuarquroy JO (})1I!S 33-008 - Jo s[(IS 3J-08 0} I *soytp ogtfo4QI {ores ;o @nfd jews 'seroo91q pus opfofy1 Jo soyIp Suny 'opmde ;o soxi( '1opdoq o1qqesoua4s yqIM aftuads as1re00 ;o SniIJ '&ikqdaod aftua4s ourfoydou poute13-9u1} 36 . I1Is 'oyru -o4s omukudaod TIS 33-001 ...... opfouoyd 30 [[IS 1J-9 *&ikqdaod afta -a4s oytoreut Jo YjIO9908T ........... eso 1914 ........ eoueq eLolg .......... TH *Ure} -unojy | OFT .......... doy, punoy YoNVTIG YHHHIS ........... seee xe94 SNIVILNAON AVINI o}TUBIL) ........ uo4us; |||||||||| x89] 9A8]) ...... uo4us; aIqIE]T YHHUMIS ||||||||| BJ9LJ BL191G ........ gy adopjuy --- -uol}¥jg |||||||| o|qBI(] 0119]) 0g 65 8G LG 95 96 F6 €6 (4A 16 08 61 SI fAl 9T 134 OCCURRENCE OF NONPEGMATITE ~BERYLLIUM IN THE UNITED STATES ©00 * ©000 © F$00 *> £00 *> £00 *> $00 *> $00 *> £00 '0> (quao12d) 0°G *o@pH qsomMqjIoU 'suor}s3 -oidos Jo sUOISNJOUL -3ad y11M oqtuo4s ;o usutoadg 'qred e1juod-q310u woIJ sUuoIsnJIUI JIM opuod4s ;o uowrdadg _ *outur uojssung Jo y3n08 nos; joures uf ouor of!} -ogi1&£d-o3114doareqo-o4114d ssouoe ordwss 3J-9°q *x2038 JO 1981 -Uuo9 14 out uojsdun} aloop(|t 18 of198} opffoayos -agoptda-;9u183 ;o (pos4reue sordwes jpouusyo g 'sSeq uswordwr7 opts som uo auo4s9u1[ UI auoz ssoroe ordures '6AI requ ssoroe ordures fouueyo 3J-9 *sseq uswordur7 do; ouo;sou[ ut 'yoor -Seu popueq 41ury} ;o sua; ssoroe ordwes fouueyo 13}-9 *FL1 xeou agnosq jou -143 poiojye pus pojeIdd9Iq ssoroe ordwres [fouueygo *x9048 JO It3U s[9J -u10y; poloyye ssorvre ofduwes 3J-p uoydjoseg *(eret) pus y3rurg {(6ret) s10u30 pus 'uosueiq 'Surst pus surepy sos 'stezop 104 ; 889 *x203s xord sgt: _u orqrew ouly ~~~(})ouojsowmt osony; -wo0 pus -~~~~~ urequnopy AM - gg SNIVILNAON MITAM LBI 981 03 PSI S61 O8T a oats" soft -uou z4renb go oxip Supp ~~~~~~ 1894 POH 28 (Coruognm pus 'of (9A . -1ou8eu 'suare3 'aqt0 -reqds oawog) opm *sdnous ¥1qSEM -sway pus 'agopida pus Jo souo3s 'zqrenb 9114984 -puss pus 'soje1a ILI-628 oyuenssois 3} QQ 0; Q -wofsuoo -~oquoruow zq1snh Jo y901g -~-~~~~~~ ye9q 1g NIVLNNON NYWKLINO _- 'on 1 4004 paprigquy yoou snoaudy vay 1 avid sordungy ponur;uo;-uo:rba3 soaa g-sun4], ay) fo qund fo sauoz jonjuoa pun sy4904 anrsnugur § «17gv], LOCALITIES IN TRANS-PECOS REGION METAMORPHIC ROCKS The limestone and other sedimentary rocks show little contact metamorphism near most of the syenitic bodies. At most places the limestone has been bleached and recrystallized, forming a zone of marble as much as 25 feet wide. Some of the marble is cut by small veinlets of dark, partly serpentinized silicates. The syenite intrusive mass at Marble Canyon, how- ever, is surrounded by a zone about 200 feet wide of white, brucite-calcite marble and akermanite-merwin- ite hornfels An inner zone of quartz-diopside and plagioclase-diopside hornfelses is found at some places. A narrower, more irregular zone borders part of the in- trusive body at Cave Peak. It consists of hornfels, with spurrite, merwinite, radiophyllite(?) and periclase, and locally contains grossularite and idocrase. At Wind Mountain and Sierra Prieta narrow zones of marble and hornfels border the intrusive bodies at a few places. At the Miller Mountain and Cerro Diablo intrusive masses much of the loosely cemented sandstone wallrock is silicified. The granite of the Quitman Mountains is surrounded by a zone of coarse garnet tactite, with or without diop- side, olivine, quartz, calcite, hematite, or magnetite (Huffington, 1943, p. 1043-1044). The tactite masses are distributed irregularly ; the largest masses are along the west-central and south sides of the Pinnacle Peak stock, in Zimpleman Pass. Here the stock is bordered by a zone 50 feet wide of coarse quartz-specularite tac- tite, surrounded by a zone, as much as 500, feet wide, that contains abundant coarse green grossularite. WIND MOUNTAIN AREA Wind Mountain, in Otero County, N. Mex., is one of the largest intrusive masses of the group that form the Cornudas Mountains of Texas and New Mexico (pl. 1). The area is most easily accessible by a graded road that turns north from U. S. Highway 62-180 at the Hueco Inn, 50 miles east of El Paso, Tex. Wind Mountain is reached by a graded road that leads south from Cornu- das Ranch to Wind Tank. The geology of the area was studied by Zapp ", who discovered eudialite-bearing syenite dikes on the west- ern side of Wind Mountain; the eudialite was later de- scribed by Clabaugh (1950). In 1944 members of the U. S. Geological Survey sampled some of the eudialite- bearing dikes and associated rocks for trace elements. One of the samples was reported to contain 0.2 percent BeQO (Fleischer and Cameron, 1946). The area was ex- amined briefly in August 1948 and was studied more thoroughly in July 1949. The earlier geologic map *' 19 See footnote 9, page 130. " See footnote 8, page 130. 135 was revised (fig. 38) and areas on the west, south, and east sides of the mountain were mapped and sampled in detail (pls. 24). GEOLOGY STRUCTURE AND METAMOBPHISM Wind Mountain is a laccolith that rises about 2,500 feet above the Diablo Plateau. It is a nearly circular dome with an asymmetrical extension to the southwest and is denuded of sediments. Talus fans on the lower slopes cover much of the contact. Dikes of several rock types are abundant near the edges of the laccolith and their attitudes are controlled by two sets of frac- tures. The main set is concentric with respect to the contact and dips inward about 30°; a less well-devel- oped set is radial and vertical. Some dikes occur in the laccolith but most are in the upturned sedimentary rocks; nearly all are within a few hundred feet of the contact. They were observed throughout a vertical range of 500 feet. The dikes are as much as 20 feet thick and fairly regular; some taper to a microscopic thinness. About 1,200 feet of limestone and shale of Permian age crop out around Wind Mountain,. The upper and middle parts are correlated with the Bone Spring lime- stone and the lower part with the Hueco limestone. The three units have not been differentiated on the geologic map (fig. 38). The Hueco limestone, as exposed at several places along the contact of the Wind Mountain laccolith, is typically gray, fine grained, and locally dolomitic. Along the western and southern edges of Wind Mountain, thin-bedded light-colored shales are exposed in the Hueco limestone. The most prominent structure of the sedimentary rocks is their doming near the laccolith where the beds dip at angles of 50° to 80° and generally are parallel to the contact. The effect of the doming may be de- tected as far as 2,000 feet from the laccolith. Metamorphism of the sedimentary rocks next to the intrusive body at Wind Mountain is variable in both extent and intensity. Bleaching and recrystallization of the limestone beds has been developed on the eastern side through a thickness of more than 100 feet (pl. 4), but elsewhere the limestone is unmetamorphosed. The shale beds of the Hueco limestone, where observed near the intrusive mass, are altered to a fine-grained brown to purple hornfels, but probably very little material was added from the intrusive body. At some localities, however, the metamorphism was accompanied by addi- tion of soda and other substances. Narrow bands of aegirite, riebeckite, analcite, and zirconium silicates border many of the dikes. At one area on the south side of Wind Mountain (pl. 3) metasomatism was 136 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES AdVLLM3L ~ $ 3? } € s $ B § # B H if. j € a Ro » B [~* § € a ine &. z § $ £ & 23 $ $ s F 3 -- #$ 3 *% w } 3 k§ §$ , C : f xlf |.; ($l Nf t WH ut [f iff C- A. : $ € - a R E 8 E 5 R. Eli # g f 3's; |§ 8&3 + $ figs € §~§ mion snur & [:' ]* & £0 a 2" puff {$ 5o if? € 3 - P B & ~" $55 {f. $. ff F & as € re $ ( snp f $ ji f $ $ $3 /s C. Timm V. R. Wilmarth, 1948-49, after 8 1941 Dsus \ . ) 2 3, if" \ as I Geology by W. T. Holser, W. 1. Finch, and R. 14 E. Datum is mean sea level FIGURE 38.-Geologic map of Wind Mountain, Otero County, N. Mex. ///l ye //// < | h ty LOCALITIES IN TRANS-PECOS REGION intense, and the sedimentary rocks are altered to a coarse tactite of epidote, calcite, and garnet. IGNEOUS ROCKS The main mass of Wind Mountain is porphyritic nepheline syenite, containing euhedral to subhedral phenocrysts of nepheline, perthite, and pyroxene in a fine-grained groundmass of 80 to 90 percent feldspar and 10 to 20 percent aegirite, Nepheline phenocrysts constitute as much as 15 percent of the rock and com- monly shows large crystal faces. The perthite pheno- erysts show a marked flow structure in which their tabular (010) form is parallel to the contact. Adjoin- ing and within a few hundred feet of the contact, the nepheline syenite has a granular texture. Phenocrysts are small or absent, and no alinement of crystals is ap- parent. Pyroxene, dominantly aegirine-augite, is pres- ent in minor quantities and is interstitial to the feld-. spar erystals. - Porphyritic rock having flow structure crop out high on the mountain and within 100 feet seem to grade into the granular syenite of the border facies. No crosscutting relations or sharp contacts be- tween these rock types were seen. The dikes that border the laccolith are highly variable in composition, but two types predominate. The more abundant is dark-green malignite that consists mostly of aegirite, with some nepheline and feldspar. This rock is generally fine grained, although in places the aegirite crystals are as much as half an inch long, and elsewhere, rectangular phenocrysts of nepheline as much as a quarter inch across are scattered throughout the groundmass. The other main type of dike rock is large- ly pegmatitic nepheline syenite ; it is rich in feldspar and contains some nepheline and aegirite. The rock is coarse grained and in places shows tabular feldspar and pris- matic aegirite crystals 1 to 2 inches in length. All gradations between malignite and pegmatitic nepheline syenite may be seen in a single hand specimen. Other dike rocks, similar in composition to the pegmatitic nepheline syenite but finer and more uniformly grained, are designated as fine-grained nepheline syenite. These may be as light-colored as the pegmatitic type, or con- siderably darker; however, the content of mafic min- erals is less than that of malignite. The best exposures of fine-grained nepheline syenite dikes are along the eastern border of the laccolith (pl. 4). A few dikes with easterly trend occur largely within the laccolith. They are dark green and porphyritic, with fine-grained groundmass, and contain inclusions of limestone and nepheline syenite. The rock is best de- scribed as a phonolite porphyry. Some of the dikes show a pronounced planar struc- ture parallel to the walls, owing to interlayering of 137 malignite, pegmatitic nepheline syenite, and fine- grained, nepheline syenite. Commonly there are only a few such layers, but at one locality (sample 329-145, pl. 3) 25 major layers and many minor ones occur in a zone about 12 feet thick. Although some of the layers are continuous for 20 feet or more, the pegmatitic nepheline syenite layers are commonly short and len- ticular. In other places masses of pegmatitic nepheline syenite are cut by malignite, and locally the rock re- sembles a breccia of pegmatitic material "cemented" by malignite. In thin section the malignite layers show a pronounced orientation of aegirite prisms parallel to the layering. The orientation is apparently the result of flow, and the lines of crystals crowd and bend sharply around feldspar phenocrysts. Most of the peg- matitic nepheline syenite dikes lack this structure, but the long axes of feldspar crystals near the dike margins commonly are perpendicular to the walls. Some of the pegmatitic nepheline syenite dikes are zoned. The zon- ing is mainly textural, although the inner unit com- monly is somewhat richer in aegirite. Planar flow structure is well developed in a dark-gray, gneissoid nepheline syenite that crops out on the south side of Wind Mountain (pl. 3). Perthite phenocrysts and albite crystals in the groundmass show orientation. The junction of a vertical dike and a flat-lying dike is exposed on the Wind Mountain claim (pl. 2). Flow lines show that the dikes were formed at the same time. Malignite and similar rocks are found near contact of both the porphyritic and granular nepheline syenite bodies with the laccolith. Their shape ranges from vague schlieren to sharply bounded dikes, but always in the same orientations. On the southern side of the mountain (pl. 3) near sample 329-622, the granular syenite of the laccolith grades imperceptibly into fine- grained syenite of a dike, and the malignite layers are similarly alined through both rocks. These observa- tions suggest that all the rock types are closely related in age and origin. The most abundant minerals of the dike rocks are feldspar, aegirite, and nepheline. The feldspars include perthitic orthoclase, albite, and minor quantities of microcline. The aegirite ranges toward augite in com- position; the outer zones of the crystals are richer in soda. Deep red-purple zirconium silicates are important constituents in some dikes and occur both in single crystals 0.5 to 3 mm in diameter and in aggregates. In places they constitute as much as 20 percent of the peg- matitic nepheline syenite. The crystals are grouped in irregular stringers and tend to be most abundant near the edges of pegmatitic layers; a few masses occur in adjacent malignite. 138 The zirconium silicates are highly variable in optical properties and in chemical composition. Purple-red crystals from the western part of Wind Mountain com- monly are color zoned about a light-brown core. Other crystals are entirely light to dark brown, some occur- ring in the same rock with the purple-red material. Some of the brown material and much of the red mate- rial is isotropic and has a refractive index of about 1.59; other brown grains show a small negative optic angle and indices near 1.62. Spectrographic analyses of three specimens from Wind Mountain are compared in table 60 with a chemical analysis of similar material from Kola, U. S. S. R. 60.-Analyses of zirconium stlicates, in percent 1 2 8 4 tree ile ganda 0. 0051 0. OOX Present 510% _ pra d 52. 12 -s. ()v E ES AVC s . 40 C103. 492: 5s bee asd o hue nota X. 0 >A 73 Deere aon eas o o ees . 63 Xt ~~ _C do : . 20 C e Asc 1. 02 2. T . OX . OX 76 LLC, 00 X _ CIL ie mt CC cs. Lt ca FOXI) {upa Sect Cos O l (2) C): %* i melnnall ne L h 2. 0 X. 0 pal 3. 46 :- she 11.8: >X. 0 >I 16. 54 "anns an s Yk a eve. Cul sores sill wed, 000X. O0 Xs :t. £ ...=. 142, " Pall coas h € 3. 74 kdl wo cal N - 9 14. 1 X. 0 pal 3. 34 148.303 __________________ X 56 Celli. s _o dO yi LLL de Cal Doll tg 0° 09 f 2k igen te DX 4144 Pele cask 2 . 06 PDAs t eca ie <. . OX +O00X: cx Ki@._. 00m LOB S - eefiut ct: t 1. 90 Ba..... c Dunes {00X st s SLW EEL HD+ cms ssa namedn webs won an oon 8. 62 00 C0 yc n ay _ Ib NUN 6. 41 ae sean)! ad I r eepan wane o ole ae None 1 Included in MgO. 2 Included in FerO;. 1. Purple-red eudialite, west side Wind Mountain. Spectrglgraphlc analysis by Saratoga Laboratories, courtesy S. E. Clabaugh; Univ. of exas, Austin. 2. Same mineral, same locality as No. 1 (sample 820-120). Spectrographic analysis by K. J. Murata. Looked for but not found: Ag, As, B, Bi, Cd, Co, Cr, Ga, Ge, In, Ni, P, Sb, Ta, Tl, V, W, Zn. 3. Brown zirconium silicate, south side Wind Mountain (sample 320-145B). Spec- tographic analysis by E.J. Murata. 4. Lovozerite, Lovozero, Kola, U. S. S. R. (Gerasimovsky, 1939, p. 754; see also Win- chell, 1951, p. 454). Chemical analysis by T. A. Burova, siectrographic analyses for U and { by I. B. Borovsky, for Be by S. A. Borovick. X-ray diffraction patterns of the zirconium silicates at Wind Mountain are similar to those of eudialite and eucolite from southern Norway and Greenland. Min- erals previously identified as eudialite and eucolite have a wide range of chemical composition (Winchell, 1951, p. 453-454). The Wind Mountain specimens differ from these minerals mainly in containing more cal- clum and less zirconium, but are probably members of a eudialite-eucolite series. -Other accessory minerals of the dike rocks include sodalite, riebeckite, biotite, apatite, and magnetite. Some of the dikes are intersected by microscopic veins OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES of analcite and other zeolite minerals; these minerals also replace some of the primary minerals. OCCURRENCE OF BERYLLIUM The distribution of beryllium in the rocks of Wind Mountain is shown on the detailed geologic maps (pls. 2-4); a few other analyses are shown on the general map of the Wind Mountain area (fig. 38). The sam- ples are described in table 61. The malignite and pegmatitic nepheline syenite dike rocks of Wind Mountain are richer in beryllium than is the porphyritic nepheline syenite that forms the main part of the laccolith. A channel sample across a typical dike, including both malignite and pegmatitic neph- eline syenite layers, probably would contain about 0.007 percent BeQ. In some samples no BeQ could be detected, and the maximum BeOQ content obtained was 0.2 percent. This value was reported for a sample (S-150-456) collected for the Mine, Mill, and Smelter Survey in 1944 from the Wind Mountain claim (pl. 2). Reanalysis of the same powder, showed only 0.074 per- cent BeO. Even this value could not be confirmed in several other samples from the same outcrop (S-150- 457 and -458; and 829-195 to -205), which gave a max- imum of 0.026 percent BeO and a minimum of <0.001 percent (pl. 2 and table 61). Although part of the discrepancy may be due to analytical errors, these analyses indicate that the beryl- lium content of the dikes and the altered rocks that border them is probably quite erratic. This is further indicated in comparing the analyses of samples from given rock types. The BeQ content in 5 samples of fine-grained nepheline syenite ranges from 0.001 to 0.022 percent, and in 7 samples of rock that is domi- nantly malignite the range is from <0.001 to 0.03 per- cent. Of the 10 samples of metamorphic rocks that were analyzed, those containing detectable amounts of BeO were all taken within a foot of a dike. However, beryllia could not be detected in some samples thus located. Analytical data for the various minerals indicate that the beryllium in the dike rocks is not contained in any particular mineral but is distributed among the feldspar, nepheline, aegirite, and eudialite. Red-pur- ple eudialite from the west side of Wind Mountain was found to contain 0.0051 percent BeOQ (table 60, column 2). A sample (329-145) of layered dike rock was separated into mineral components by heavy liquids, and a spectrographic analysis was made for each of the separates. The aegirite separate contained 0.000X BeQ, the zirconium silicate 0.00X percent, and the combined nepheline and feldspar 0.003 percent. Two separate quantitative analyses of parts of the sample showed 0.0074 and 0.001 percent BeQO, neither LOCALITIES IN TRANS-PECOS REGION Tasus 61.-Beryllia in samples from Wind Mountain 1839 [Key to analysts: KJM, K. J. Murata; JDF, Janet D. Fletcher; JTR, J. T. Rozsa, National Egyectrogmphic Laboratories, Inc.; L WS, L. W. Strock, Saratoga Laboratories, Inc.; MMS: samples collected and analyzed by Mine, Mill, and Smelter Survey. MMS spectrographic} Sample 320-128 129 132 135 136 145 145A 145B 1450 149 150 151 153 156 157 195 196 197 198 199 200 201 202 203 204 205 605 607 611 615 619 620 622 631 632 633 649 652 B-150-456 457 458 of which can be reconciled with the values obtained for the mineral separates. Although the accuracy of the results may be challenged, some of the discrepancy may have resulted from erratic distribution of beryl- Plate show- ing locality nto +n Co _ wh wh bo bo bo Description Specimen of malignite dike with large nepheline Separate of eudialite from pegmatitic nepheline syenite, near 329-128-.____.-_-- 4-ft channel sample across hornfels altered to Clay-.-.------_--_--------------- 3-ft channel sample across eudialite-bearing fine-grained nepheline syenite dike. . 1-ft channel sample across thin eudialite-rich pegmatitic nepheline syenite dike and bordering (owe e Edem old os a bins 3-ft channel sample across lower part of 20-ft dike of banded nepheline syenite pegmatite, fine-grained nepheline syenite, and malignite, containing zirconium 2 ..... . 22 nl alee ne 2a ae o moe an e e me he he d te md mh e me mee e et n i y def an ariel as os n e an he in he ie a ia s Separate of aegerite from Separate of brown zirconium silicate from gag-145 ~. Si Nepheline and feldspar from Specimen of malignite dikes in porphyritic nepheline syenite_-_._----_------.--- Tab sample from thin serpentine vein in hornfels-______-_---_---_------------ 4-ft channel sample across magnetite-bearing hornfels, some altered to clay.... Grab sample of alteration zone in limestone near northwest corner of figure 38, containing quartz, chalcedony, siderite, and iron and manganese oxides._____.. Specimen of 3-in. coarse malignite dike in granular. syenite. cl lus Grai) sample of 6-ft banded dike, predominantly malignite with brown zirconium SHCALE... <....) annees nosso names Channel sample across 15-in. altered shaly limestone....--_--._----~----------- Sample from two 1-ft channels across thin, gray, fine-grained nepheline syenite dike, immediately below 329-195... Samgle from three 14-in. channels across black hornfels immediately below $20 196.1 _ L. c 220 LOE O_O noe a aa me - aon a am mle ain a Cena's as Broad 1-ft channel sample across limestone, from same locality as 829-197...... Channel sample across 6 in. of porcelainic limestone, near hanging wall of flat- lying banded dike (829-202) ___ Chg}; saéglfle of dark-green aegirite hornfels along hanging wall of same dike as § BOR. 2 cll. e ae ue m o aime l mle l mee as o i ie raid a 0 he al s Ie t im t aa in a ae in min ha dn he in ms m tet ne in toe in Same ON fOOtWAILL Chip sample across flat-lying banded dike, same locality as 329-199 to 201... Chip sample of vertical banded dike with some very coarse feldspar. Some horn- fels Specimen of GTANUIAT Specimen of anthophyllite asbestos lying between dike rock and aegirite hornfels.. b-ft Ehannel sample across banded eudialite-bearing dike.__________________---- . i e i i i i a n i i ii C e Sa o c A e rel ul oar ye Composite of four specimens of porphyritic nepheline syenite from borders of main part of IACCOlith. _ 6-ft channel sample across banded malignite and 2.5-ft channel sample across fine-grained nepheline syenite dike._.__...---.--..- 2-fgzghzngel sample across limestone and hornfels at footwall of dike sampled in Lds o ce e e at mere a a mee et o o ch e ap e tale In he e on ho soient ie al e ae in in Is oe irr is to on e ae me a mae son a i a a in in Channel sample across metamorphic rocks at contact porphyritic nepheline sye- nite, including 10 ft of epidote tactite and 5 ft of calcite marble.___________-- 15-ft channel sample across unaltered limestONn@_________________.-_-_--_____~ 15-ft channel sample across leucocratic fine-grained nepheline syenite........... 10-ft channel sample across fine-grained nepheline syenite at contact with por- phyritic nepheline Chip sample across 25-ft outcrop of gneissoid nepheline Specimen of phonolite porphyrg with limestone and syenite hip sample across 0.8 ft of hard altered limestone, with two small eudialite- bearing malignite dikes, same locality as 329-195 to il- Chip sample across 2 ft of eudialite-bearing malignite dike, same locality.... Chip sample across 6 ft of same type of rock, same locality _. c_L gravimetric analysis by Mine, Mill, and Smelter Survey; BeO (percent) 0. 014 . 0051 | <. 004 . 0065 . 008 <. O01 . 022 . 012 . 001 <. 001 . 001 . 0068 . 008 . 005 . 0063 . 022 . 0013 . O01 . OOOX . 0072 . 0063 . 004 . 004 074 14 a <. O01 <. 001 all other analyses Analyst JTR KJM LWS LWS JDF The dikes range in thickness from less than an inch to as much as 20 feet and in length from 5 feet to at least 300 feet. Though largely covered by talus, they probably are present throughout a zone a few hundred lium in the minerals. An unsuccessful search was | feet wide extending around the 5-mile circumference made for the beryllium minerals, such as helvite, eudi- dymite, meliphenite, and leucophanite, that occur in pegmatitic nepheline syenites in southern Norway. be recovered. of the Wind Mountain laccolith. Thus, they would represent a substantial reserve if their beryllium could 140 CAVE PEAK AREA The intrusive complex at Cave Peak is in the Sierra Diablo, about 35 miles north of Van Horn, Tex., and 2 miles west of State Highway 54 (pl. 1). Though Cave Peak is about 1,300 feet above the alluvial floor of Salt Basin, it is overshadowed by the cliffs on the eastern scarp of the Diablo Plateau. The intrusive rocks of the Sierra Diablo region were first mapped by Richardson (1914). Later King and others of the Geological Survey mapped the sedimen- tary formations and structures of the region (King and Knight, 1944; King, 1949). The uncommon igne- ous rocks of the Cave Peak area collected by King were studied by Charles Milton, Earl Ingerson, and others. In 1944 the Cave Peak area was sampled by A. L. Slaughter for the Mine, Mill, and Smelter Survey. Two samples from one of the prospect pits contained 0.3 to 0.02 percent BeOQ. Because of the unusual quantity of beryllium reported in these samples, the geology in the vicinity of Cave Peak was mapped in detail during the present investigation (pl. 5). GEOLOGY The igneous rocks of Cave Peak form an intrusive complex that is nearly circular in outline and about half a mile in diameter. The rocks are mainly light and dark rhyolite porphyries and breccias. The central core of the complex is a plug of porphyritic granite about 300 feet in diameter. The complex resembles a- volcanic neck but no lavas are found in the region. The ringlike structure of the various rock types around a core of granite (pl. 5) suggests that the pluton intruded almost to the surface. Porphyritic syenite that is more like the igneous rocks found elsewhere in the Trans-Pecos Region forms the intrusive mass at Marble Canyon, a mile southwest of Cave Peak. The relation of this mass to the complex at Cave Peak is not known. ._ Most of the sedimentary rocks intruded at Cave Peak are dark-gray, thick-bedded limestones of the Hueco limestone (Permian). Near the southwestern side of the intrusive body, the Hueco limestone grades upward into the black limestone of the Bone Spring limestone (Permian). The formations are similar in appearance and were not differentiated in mapping. The limestone near its contact with the intrusive mass is largely calcite, but some beds are dolomitic. The rocks dip 2° or 8° to the south over much of the area, but are highly de- formed within a few feet of the intrusive mass. Where observed, the strike of these deformed beds is approxi- mately parallel to the contact, and dips range from nearly vertical to 35° toward the mass. On the south- west side of Cave Peak there is faulting along the con- OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES tact, as indicated by a breccia zone several feet thick and slickensides. IGNEOUS ROCKS The most abundant rocks are breccias, composed mainly of fragments of rhyolite porphyry. Nonbrec- ciated felsite, mainly rhyolite porphyry, are less exten- sive in outcrop. The branches are subdivided on the basis of color into light rhyolite breccia and dark rhyo- lite breccia. The porphyries are similarly subdivided into light and dark rhyolite porphyry. Field relations suggest that the light rhyolite porphyry is probably the oldest intrusive rock and light rhyolite breccia the youngest, except for a few late porphyry dikes. The dark rhyolite porphyry and breccia are of intermediate age, the breccia being somewhat the younger of the two. The central core of granite appears to be younger than the dark rhyolite. Light rhyolite porphyry occurs as dikes and irregu- lar masses mainly in a zone about 400 feet wide around the southern end of the intrusive mass (pl. 5). The rock is largely greenish gray and is aphanitic except for scattered phenocrysts of feldspar and quartz as much as 3 mm in diameter. It weathers light gray. In places other varieties of felsite are associated with the light rhyolite porphyry and were undifferentiated from it in the mapping. In several outcrops on the south- eastern slope of Cave Peak and in the large outcrop on the western ridge, the rhyolite contains no phenocrysts, but it is otherwise similar to the porphyry and appears to grade into it. Locally the rock contains no quartz and is probably trachyte or andesite porphyry. The dark rhyolite breccia and porphyry are best ex- posed in a circular area on the northern slope of Cave Peak. The dark-gray to black, fine-grained rhyolite porphyry contains abundant feldspar and a few quartz phenocrysts about 2 mm in diameter. Microscopic ex- amination by Charles Milton indicates that the feldspar is a slightly albitized orthoclase, and that the ground- mass is orthoclase, quartz, biotite, and a little sphene (P. B. King, 1948, written communication). The dark- gray rhyolite breccia is composed largely of randomly oriented angular fragments as much as 2 cm in diam- eter. Some of the fragments are similar to the dark rhyolite porphyry. The inclusion of porphyry frag- ments in the breccia indicates that the breccia is younger. Near the contact of the dark rhyolite porphyry with the porpyhritic granite, the porphyry is brecciated, silicified, highly altered, and crisscrossed by innumer- able tiny quartz veins. The resulting rock is hard and medium- to fine-grained ; the colors are light shades of pink, gray, and green. Where replacement is complete, parts of the rock closely resemble aplite, but in other LOCALITIES IN TRANS-PECOS REGION places remnants of the rhyolite porphyry texture are preserved. The altered zone forms an aureole around the granite plug, suggesting that the alteration is re- lated to emplacement of the granite. The porphyritic granite is a dense medium-grained rock of quartz and orthoclase crystals in a fine grained groundmass of similar composition. It contains rare green skeletal crystals, possibly epidotized remnants of biotite; otherwise mafic minerals are lacking. Orthoclase is opaque white from slight alteration, and the rock is partly replaced by manganese and iron oxides. Light rhyolite breccia underlies most of the main ridge and is the most abundant rock in the area. It crops out in a ringlike zone about 600 feet wide. The rock is pale orange and consists mainly of angular frag- ments of rhyolite in a felsitic groundmass of quartz and feldspar. Many of the fragments are like the ground- mass, others are rhyolite porphyry with conspicuous flow structure, and a few are metamorphosed limestone. The areas of dark breccia that occur near the top of the peak may be large blocks of dark rhyolite breccia like that of the north slope, or a darker phase of the sur- rounding light rhyolite breccia. Fragment size varies widely from place to place. On the eastern side of the peak near the outer contact the light rhyolite breccia is composed of fragments as much as 2 meters in diameter, but near the inner contact the average diameter of frag- ments is less than a centimeter. The zones of contact, as well as the character of the inclusions, suggest that the light rhyolite porphyry is the last of the larger in- trusive bodies. METAMORPHIC ROCKS The limestone on the eastern and southern sides of Cave Peak has been metamorphosed to marble or horn- fels in a zone as much as 150 feet wide that has been cut by dikes and irregular masses of light rhyolite porphyry. Nearly all the exposures of rhyolite por- phyry are surrounded by an inner zone of hornfels not more than 50 feet wide and by an outer zone of marble. These zones indicate that the metamorphism was related to the intrusion of porphyry. The mineralogy and petrography of the metamorphic rocks are complex. The limestone is mostly meta- morphosed to a white to buff, fine-grained marble that locally contains some fine white needles of tremo- lite(?). Chert nodules in the marble are altered to a green silicate rock that probably contains diopside. The areas mapped (pl. 5) as hornfels include a va- riety of rocks. A common type is a light-gray or white, very fine grained hornfels that according to Charles Milton is principally spurrite (CaCO;:2Ca,8i0,) and 141 merwinite (Ca;MgSi;0;) with a little periclase (MgO). Another type is a greenish-brown hornfels that is at least in part grossularite, idocrase, and wollastonite. The presence of spurrite and merwinite indicates meta- morphism at very high temperature (Bowen, 1940, p. 255-264) and comparatively low pressure (Korzhinsky, 1937). The association of wollastonite-garnet-spurrite is also in this same temperature range (Yoder, 1950, p. 249). The principal constituents of the white and gray hornfels are silica, lime, and magnesia, according to chemical analyses (table 62). TaBu® 62.- Analyses of hornfels from Cave Peak [K. J. Murata, analyst] 1 2 Insoluble: ... : sk 6 . 28 (S10) -_. (3. 60) (1. 00) SIO». o>. co t YELL. aR aa in ass 25. 38 . 56 RO.: fc _. Lsd cl cl 1. 62 2. 80 sas is- 5. 93 3. 06 Cao ~. :: aao a R 55. 00 54. 04 - NMEA A aaa dee fae oa o 5. 95 7. 00 : ae Ru- - 2. 03 2. 09 HO~- .... ._ « o cee sn allan Loe . 29 . 09 prom Loo l Moc. [L eas ual LBI < . 06 SOA LIE SALE UIE rang , . 14 None(?) 100. 11 99. 97 LLCT sual... . 06 . 02 100. 05 99. 95 1 Corrected for oxygen equivalent of fluorine, 1. White hornfels from east side Cave Peak, containing spurrite, merwinite, garnet, wollastonite, idocrase, calcite, etc. P. B. King's specimen 7O7A. $. GgggBhornfels, principally spurrite, from same locality. P. B. King's specimen Both the hornfels and the marble are crisscrossed by thin veins of fine-grained, hard material, ranging from white to light green. Similar material was determined by Charles Milton as thaumasite (CaSO, CaCO, CaSO, - 14.5H.,0) and calcite. Also, he noted the alteration of much spur- rite and merwinite to a hydrous silicate that is prob- ably the rare mineral radiophyllite, (CaO SiO; +H,0). These hydrous minerals undoubtedly represent a retro- gression from the intense initial metamorphism. On a weathered surface the metamorphic rocks and their veins are altered further to claylike material. OCCURRENCE OF BERYLLIUM The samples analyzed for beryllium are described in table 63 and their localities are shown on plate 5. On the eastern slope of the peak a 4-foot-thick shear zone at the face of an adit has brought a block of altered light rhyolite porphyry into contact with the light rhyo- lite breccia. The rock in the shear zone is completely altered to clay, iron oxides, and gypsum. At the portal of the adit a 1-foot shear zone separates the block of porphyry from hornfels. 142 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 63.-Berylia in samples from Cave Peak, in percent [All analyses spectrographic except as noted. Analysts: KJM, K. J. Murata; JDF. Janet D. Fletcher; JTR, J. T. Rozsa, National Spectrograhphic Laboratories; L WS, L. W. Strock, Saratoga Laboratories, Inc.; MMS, Samples collected and analyzed by Mine, Mill, and Smelter Survey] Sample Description BeO Mo Nb Pb En Zn Analyst 829-017a Sample from two 1.5-ft channels across limonite vein with steep westward dip in dark rhyolite por- phyry and breccia, at portal... _ __ 12: 1 (mento cloe det reale aid ce al- fap ania ca re bile dalle LWS 020 Channel sample across 7 ft of highly © altered, banded rhyolite porphyry dike, some quartz, limonite, and manganese oxide replacement. ._ __ [C ! rasi o sra oar ae faa aoe. LWS 021 - Chip sample of 3-ft light rhyolite dike f altered to clay and hematite _ ___ <. 004 "g- sinemet nie ain ales aL can't - T beret sn bae LWS 054 Channel sample across 2 ft of hema- tite-bearing fracture zone in dark rhyolite porphyry, at portal of hdib? ©.. : bene _ l tpa ao" i" LWS 055 Channel sample across 6 ft of hema- f tite-bearing fracture zone in dark thyolite breccia... 2. {_n canis "" ir to at al Ate LWS 056 Chip sample across 6 ft of hema- tite-bearing fracture zones in light rhyolite . .:004 0 O mate" t _ anl mr r is aed ba ~- LWS 057 Channel sample across 6 ft of hema- tite and limonite vein, 20 ft inside adit in light rhyolite breccia. __.. _ __ .m f tt" _ Ja fla tobi l "de GAM -LWS 062 Channel sample along small fracture $ zone bearing iron oxides, in pros- , pect shaft indurk rhyolitebreccis. . <(.004. - .____l. "0.0 "_ no - aoi Nao LWS 064 Chip sample across 6-ft wall of adit (35 ft in) veined with iron oxides copper carbonates, fluorite, and minor wolframite in light rhyolite breeelg. c-. R 32 004 s Tola Aneto at aol. LWS 065 Chip sample of 0.3-ft vein similar to 329-064, at portal of adit ._______ 1.004" -i _ sleet ai boc tarde o. nath. a LWS 074 - Grab sample of various types of horn- ( fels, near 829-206. ___ .001 ; csi _c {Af rtx co f {ioral tnmnj ar _ JTR 077 Channel sample across 4 ft of shear zone altered to limonite, clay, and gypsum, at contact of light rhyolite breccia and altered light rhyolite porphyry, near face of adit____ ___. . O1 0. OOX 0. OX 0. X 0. OOOX 0. OX JDF (. 0096) : LWS 078 Channel sample across 6 ft of altered light rhyolite porphyry, between 829-077 and portal..___.._____~__ . 004 . OOX . OX . OX . O0OO0X . OX JDF (. 0063) LWS 079 1-ft channel sample across 1-ft shear zone altered to limonite, clay, and gypsum, at portal.: _-....__...... . O1 . OOX . OOX xX . O0OX tw.d JDF (. 017) ! LWS 080 Channel sample across 3.5 ft of gray hornfels containing grossularite, spurrite, etc., next to portal__ ___ __ #. 004) :s. act _" f in 0 Pur amalr o Sint a LWS 081 - Channel sample across 15 ft of black hornfels containing spurrite, etc., with many greenish-white veins, outward of 329-080..___________ 73. 4 a. ma cL de tart ame du l dent anl aafes 2s LWS 084 Specimen of pink hornfels._________ <. [e mi sora i avy aut tate I arr JTR 206 - Chip sample across hornfels area_____ [001N 2.0. coli" wor t oar mb on TP.. JTR 208 Chip sample across feldspar-bearing hornfels. . . colar ...l £001 2s a aries seral non ie o Aotea ( t a JTR 209 Chip sample across small hornfels in- L2 :2 + 22 cya e erase cl ages ae adOI.! :s i asset sheds ii aan an ao, JTR 680 Chip sample across 25 ft of grossu- 5 larite-idocrase-spurrite(?) hornfels. . 0005 «ci00®% ' If _ so.} <. 000X _ <. OOX <. OX JDF 682 Channel sample across 3 ft of rhyolite breccia near 329-680..._____L___. seis retailers eau t an . aaa o. JDF 684 Chip sample of hornfels_.___________ 00018 c_. clo o arcana c rou to JDF 685 - Chip sample of light rhyolite breccia, , near _: £10040. 5 Golfe hile ae s tian, Joo Roane JDF 686 Chip sample of light rhyolite por- phyry, near 329-685 and 685... _ ___ &: 0001 4, - ror ie e e! en een ra bee b e d cn meee deinen ches JDF See footnotes at end of table, LOCALITIES IN. UTAH 1483 Tasos 63-Beryllia in samples from Cave Peak, in percent-Continued Sample Description BeO $-150-448 - Channel sample across 1.5 ft of brec- ciated contact rock, gypsum-rich and iron-stained (same as 329- O0TT?. .cc... s Gee mass 0. 3 (. 082) ! 449 - Chip sample across 12 ft of brecciated gray-green porphyry (same as 329- 120 +8 078 and 0:9?)“1: estar bare ts . 02 pecimen of purplish-gray porphyry in adit (same as $29-057?7)_ ___ -- -- <. O01 451 - Channel sample across 1.0 ft of pur- plish-gray porphyry with manga- ESOS: ac- «} <. 001 452 - Channel sample across 1.3 ft manga- nese-bearing vein......--------- <. 001 516 Grab sample of brown porphyry with manganese stains, from dump, comes with <. O01 517 - Chip sample of hard siliceous breccia. <. O01 518 - Channel sample across 5.4 ft of light- gray rhyolite porphyry dike_...... <. O01 519 Channel sample across 8.0 ft of por- phyry ... dna <. 001 520 Channel sample across 6.0 ft of light- brown fractured porphyry (same as <. 001 1 Analyses in parentheses made on a split of the sample. 2 Chemical analysis. Analyses of samples (329-077 and -079) from the shear zones in the adit showed 0.0096 to 0.017 percent BeQ and as much as 0.X percent Pb, 0.X percent Zn, and 0.0X percent Nb. The minerals containing these elements were not identified. The altered light rhyo- lite porphyry (sample 329-078) contains less of these elements. A sample (S-150-448) taken earlier from the shear zone at the adit face was reported to contain 0.3 percent BeQO, but reanalysis of the sample showed only 0.082 percent. Samples of the rocks adjoining similar shear zones several hundred feet north (829- 685) and southwest (829-682) of the adit contained 0.0049 and 0.0076 percent BeQ, respectively. Beryllium apparently is confined to the shear zones and the rocks adjoining them, as none was found in the many samples of other rocks taken from various parts of the area. Although the average beryllium content of the shear zones appears to be relatively high, the zones can be traced for only a few tens of feet, and their aggregate tonnage is probably small. f UTAH By L. A. WarnrEr and V. R. Information on the BeQ content of nonpegmatite rocks in Utah was obtained at 6 localities (see fig. 89). In September 1949 we investigated and sampled the beryl-bearing granite in the Sheeprock Range and the ore deposits associated with contact zones in the Tintic, West Tintic, and Ophir mining districts. Samples Mo Nb Pb Sn Zn Analyst 0. 02 «30.001 ~......_L-2 .:: -:..%~>. MMS KJM . O1 200. ©: sys cue 009. : .. MMS . 8 1 ss luigi. cs i PVA ita ders MMS . 8 04 ! .s we- (O2 a isk MMS (. 17) G t 4 OB rel tere ntp - "S09 _ i 2 uel s. MMS ________ <©c.001 . cli MMS ________ <. 001) {n ail MMS ________ i001." ~ MMS ________ «£. 001 fies Lue " ace.~ s MMS ________ «X 00L z.. JAA sites ella MMS from the Little Cottonwood district were furnished by T. S. Lovering. The beryl-bearing rhyolite at Topaz Mountain in the Thomas Range had been sampled pre- viously for the Geological Survey by J. C. Olson. With the possible exception of the deposits in the Sheeprock Mountains, none of the others investigated seem likely to furnish beryllium. However, the occur- rence of beryl in igneous rocks at two widely separated localities in west-central Utah holds some promise that beryllium deposits may be discovered in this region. JUAB AND UTAH COUNTIES TINTIC DISTRICT The Tintic district is on the boundary between Juab and Utah Counties about 60 miles south of Salt Lake City in the central part of the East Tintic Mountains. Descriptions of the geology and ore deposits of the dis- trict have been given by Tower and Smith (1899), Smith, Tower, and Emmons (1900), Crane (1915; 1923), Lindgren (1915), Lindgren and Loughlin (1919), Parsons (1925), Hunt (1928), Farmin (19833), Park (1935), Kildale (1944), and Lovering and others (1949). A brief examination was made of contact metamor- phic deposits at the Black Jack and Dragon Iron mines and near the Carisa stock, all in the central part of the Tintic district and about 1 mile east of Silver City. The Black Jack mine, half a mile southeast of Mam- moth, is in metamorphosed limestone near the contact with an altered monzonite dike. In an opencut a black 144 OCCURRENCE j 42° I--_.--_-- m a ho 110° r EXPLANATION 42° | i e Locality sampled for this report x3 Other sampling. l...\—.._.___ 40° tex a i os st sven to co Remer is i 38° ( Annie \ 112° 110° 40 ? f I 1210 Miles DISTRICTS Juab and Utah Counties 1. Tintic district 2. West Tintic district 3. Topaz Mountain Salt Lake County 4. Little Cottonwood district Tooele County 5. Ophir district 6. Sheeprock Mountains FIGURE 39.-Index map of Utah, showing localities sampled. manganese-stained siliceous rock is next to a zone of altered monzonite that is composed of clay and quartz. A grab sample (828-929) of the altered monzonite con- tained less than 0.0001 percent BeQO. The Dragon Iron mine is on the north side of Dragon Canyon about a mile southeast of the Black Jack mine. The mine is in metamorphosed Ajax and Opohonga limestones of Ordovician age near their contact with a monzonite stock. A northwestward-trending zone of altered rock that is rich in limonite extends for about a thousand feet along the contact of the stock and is ex- posed in a large opencut. The margins of the zone are largely kaolin. Grab samples were taken of iron ore from the dump (828-926) of altered limestone from the north edge of the opencut (328-927) and of kaolin from the south edge of the opencut (828-928). All contained less than 0.0001 percent BeQ. The Carisa stock, a small monzonite body 2,000 feet in diameter, is about half a mile northeast of the Dragon Iron mine. Near the contact, the Bluebell (Sil- OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES urian and Devonian) dolomite has been changed to a spinel-garnet-pyroxene rock. A grab sample (328- 925) of this rock from the southwest side of the stock contained less than 0.0001 percent BeQ. WEST TINTIC DISTRICT The West Tintic district covers an area of several square miles in eastern Juab County about 25 miles airline southwest of Eureka. The geology and ore de- posits were studied by Loughlin (Butler, and others, 1920, p. 482-444) and Stringham (1942). Precambrian shale, conglomerate, and quartzite are in fault contact with, and unconformably underlie dolo- mite, limestone, quartzite, and shale of Paleozoic age. These are intruded by granodiorite and monzonite stocks and dikes of Tertiary age. Tertiary rhyolite flows cover the sedimentary rocks east of the district. Contact metamorphic and fissure-vein deposits in the limestone of Paleozoic age are related genetically to the intrusive granodiorite and monzonite. Gold, silver, lead, copper, and tungsten are the principal metals pro- duced. A brief examination was made of the Iron King and Desert Tungsten mines. The Iron King mine, in the western part of the dis- trict, is in a narrow tactite zone in limestone. Mag- netite and specularite are the principal ore minerals. f Garnet, epidote, diopside, tremolite, and quartz replace the marmorized limestone adjacent to the iron ore. A. grab sample (328-930) of monzonite was obtained from an exposure 300 feet west of the mine, and a grab sample (328-931) composed of garnet, epidote, quartz, diopside and magnetite was taken from the mine dump. These samples did not as much as contain 0.0001 per- cent BeQO. The Desert Tungsten mine, about 1,000 feet east of the Iron King mine, was operated during World War II for tungsten. Scheelite occurs with garnet, magnetite, epidote, and some tremolite, in a fissure vein in lime- stone. A grab sample (328-932) from the dump did not contain as much as 0.0001 percent BeQO. TOPAZ MOUNTAIN, THOMAS RANGE By J. C. Orsox Pink beryl occurs in the topaz-bearing rhyolite of Topaz Mountain in the Thomas Range, Juab County, Utah. The best known locality for topaz and beryl is nearly 2 miles south-southeast of the summit of Topaz Mountain, at an altitude of about 5,700 feet, and is about 40 miles northwest of Delta, Utah, by good dirt road. The pink beryl on Topaz Mountain was first men- tioned by Hillebrand (1905). Patton (1908) described the topaz and bixbyite in the rhyolite, but did not men- LOCALITIES IN UTAH tion the beryl. He states that topaz is scattered through the rhyolite for several miles, but is most abundant on Topaz Mountain. Palache (1934, p. 14) described the beryl as follows: Beryl: This mineral, so unfamiliar in such surroundings, has been reported recently from this locality under the name of apatite. A considerable amount of blasting yielded only a small number of specimens. It is in the form of small crystals of a rose-red color attached to the cavity wall or to topaz. The crystals are tabular, simple combinations of prism and base, and rarely reach a diameter of 5 mm and a height of 3 mm. The color is a delicate pink and somewhat variable. Under the microscope the crystals show a zonal structure, the zones hav- ing slightly varying optical properties. They enclose tiny quartz crystals. I am indebted to Mr. Harry Berman for the following optical data. The crushed crystals show a variation in refractive index w=1.580+ to w=1.570+. This variation is due apparently to zoning. The average values are w=1.576, e=1.570. These values indicate a beryl low in alkalies. The specific gravity 2.67+.01 likewise indicates a low alkali content. The topaz is comparatively abundant as clear color- less crystals in cavities in rhyolite that occupies an area at least a mile wide and several miles long. At the principal workings for topaz, about half a mile north- west of the camp maintained by the Utah Geological and Mineralogical Society, the rhyolite has been blasted at about four places over a distance of 1,000 feet. Topaz is common both in the rock quarried and throughout much of the other rhyolite in the area, but beryl is diffi- cult to find. Beryl occurs as very rare, quarter-inch or less, tabu- lar pink crystals. The richest locality found in a day's reconnaissance is a small pit dug for specimen material. A half-hour search at the pit yielded only 3 tiny crys- tals. Because the visible beryl is such a minute per- centage of the rock, spectrographic analyses were made of 7 samples of rhyolite in which no beryl was visible. A sample of massive rhyolite containing no large cav- ities, from about 600 feet north-northwest of the camp, contained 0.0011 percent BeQ. Samples from three of the localities where rock was blasted for topaz con- tained 0.0020, 0.0012, and 0.0020 percent BeQ. Two samples of rhyolite from the pit dug for specimen beryl contained 0.0039 and 0.0020 percent BeQ, and a sample of rhyolite 100 feet northeast of the pit contained 0.0021 percent BeO. The 7 samples range from 0.0011 per- cent to 0.0039 percent BeQ, averaging 0.0020 percent, which appears to be a representative figure for this large mass of rhyolite. SALT LAKE COUNTY LITTLE COTTONWOOD DISTRICT The Little Cottonwood mining district is between the Big Cottonwood and American Fork districts in the 145 central part of the Wasatch Mountains, just southwest of Park City. The geology and ore deposits of the region have been described by Butler and Loughlin (1916). Rocks of the area include Precambrian quartz- ite and slate that are overlain by formations consisting of limestone, shale, and sandstone of Paleozoic and Triassic ages. These rocks were intruded by stocks and dikes of granodioritic quartz diorite. Tactite de- posits formed locally in the limestone beds. The prin- cipal ore deposits are lead-silver veins and replacement bodies. f Two grab samples of tactite, containing idocrase, quartz, and garnet, from an unidentified locality in the Little Cottonwood district were furnished by T. S. Lovering. They contained less than 0.0001 percent BeQ. The district was not visited by the writers. TOOELE COUNTY OPHIR DISTRICT The Ophir district is on the west side of the Oquirrh Range, about 30 miles southeast of Tooele. Loughlin (1917), Butler (Butler and others, 1920, p. 3874-382), Wichman (1920), and Gilluly (1932, p. 139-156) have described the geology and ore deposits of the district. The rocks are largely sedimentary and consist of quartz- ites, shales, and limestones ranging in age from Cam- brian to Carboniferous. The igneous rocks are highly altered and occur as small dikes and sills in the sedi- mentary formations. Lead and silver, with minor amounts of copper, zinc, and gold are the principal metals recovered, mainly from replacement bodies in limestone. In some places the limestone has been al- tered and replaced by epidote, quartz, sericite, and orthoclase. A grab sample (828-924) consisting of marble, epi- dote, and silicified limestone collected from the dump of the U. S. mine did not contain as much as 0.0001 percent BeQO. SHEEPROCK MOUNTAINS The Sheeprock Mountains are in southeastern Tooele County and northeastern Juab County about 25 miles west of Eureka, Utah. Beryl-bearing granite occurs in the northern part of the range north of the Ekker Ranch. The area is accessible by gravel and dirt road extending northwest from Jericho on U. S. Highway 6, 20 miles south of Eureka. Two days were spent studying the occurrences of beryl and exploring the granite boundary for tactite deposits. Little detailed work has been done in the Sheeprock Range and the general geology is known. Butler and others (1920, p. 423-426) made a reconnaissance survey of the region, and the Precambrian rocks were de- scribed by Eardley and Hatch (1940, p. 823-827). , 146 These rocks appear to constitute the bulk of the range and consist largely of quartzite with some phyllite and a few conglomeratic layers which may be of glacial origin. Limestones and quartzites of Paleozoic age crop out in the West Tintic district at the southern end of the range and in parts of the Columbia and Erickson districts at the northern end. The principal intrusive 112°15 112°30' 40°00' ax ee 4~ $ & 2 Z U 22 3) [& WEST TINTI wo "I ($ DISTRICT > > > tn I, Jericho Ii-39°45/ Geology after Butler and others, 1920, fig. 46 EXPLANATION SEDIMENTARY ROCKS U & 8 &\\\ }3 Limestone and quartzite ) 7 o_ # is Lu on Quartzite Five IGNEOUS ROCKS + + x ( Sy Rhyolite porphyry fig N 33 [Sf als Isl < Granite & Contact Approximately located 110 Miles s Sf i F1iGuRE 40.-Geologic index map showing locations of areas investigated in Sheeprock Mountains, Utah. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES rock is the beryl-bearing granite stock which extends nearly across the northern part of the range, cutting both Precambrian and Paleozoic rocks. The general geology of the region and locations of the area we in- vestigated are shown in figure 40. Beryl is sparsely distributed through granite and aplite near the central part of the stock about 1 mile north of the Ekker Ranch house (see fig. 41). The major occurrences are in an irregular zone extending for nearly 2,000 feet along the east side of Hard-to- Beat Canyon. The beryl is a bright blue with index (No) of 1.58, indicating about 13 percent BeO. It occurs as rosettes and single crystals along poorly de- fined fractures, veinlets, and schlieren which appear to be related to the flow structure in the granite. Rosettes are fairly common and some are as much as 6 inches in diameter, with beryl crystals radiating from the center. One piece of beryl float showed comb structure, with beryl crystals perpendicular to the walls of a fracture filling. Other occurrences consist of small irregular aggregates of beryl with quartz and feldspar which form isolated pods and lenses in the granite. Tex- turally these aggregates resemble pegmatite, though pegmatite dikes were not noted in the area examined. Much of the beryl, particularly in the aplite, occurs as single crystals or small groups of crystals less than a centimeter in diameter, In most places the beryl ag- gregates are separated from their nearest neighbors by several feet to several tens of feet of apparently barren granite, and large parts of the zone appear not to con- tain beryl. Thin sections of the granite reveal that its mineral composition is approximately 35 percent perthite, 30 percent albite, 25 percent quartz, 5 percent biotite, and 5 percent orthoclase and miscellaneous constituents. The composition of the albite is about Abs;, correspond- ing to that of the blebs in the perthite. A few grains of albite-antiperthite, containing blebs of microcline, were noted. Perthite was the latest mineral to form, filling interstices between the other minerals. The bio- tite is pale, highly pleochroic, and strongly birefrin- gent. It contains inclusions of zircon which show well- developed pleochroic halos. Mineral composition of the aplite is similar to that of the granite except that orthoclase is abundant and perthite is absent. A thin section cut from a specimen of beryl-rich granite, showed beryl interstitial to corroded grains of quartz and albite; perthite and orthoclase were lack- ing. A section cut from adjoining beryl-free granite showed abundant perthite interstitial to uncorroded grains of quartz and albite. It seems clear that the beryl replaced perthite and orthoclase. This evidence, together with the field relations, suggests that the beryl LOCALITIES IN UTAH 147 I + [+4 e} Z u 2 o p- ti fnk +4 t~-.. a_. $ a48:93? Meis 328 - 934-935. Contact ~ / Gossan 80 -s Vein, showing dip Dashed where inferred Geology by L. A. Warner Strike and dip of beds and V. R. Wilmarth, _aZ5 September 1949 Strike and dip of foliation fue: Adit ® Shaft X Pit 1000 o 2000 Feet T s2e-o42 eevee | | Locality sampled and number Fiaur® 42.-Geologic sketch map of northwest contact of granite stock, Sheeprock Mountains, Utah. morized, but no tactite was found. A few fissure de- posits containing quartz, pyrite, chalcopyrite, limonite, and in places magnetite, were formed in the granite and adjoining rocks. A veinlike deposit along the west margin of the granite has been oxidized to a gossan that was traced for more than 1,000 feet. A sample of this material (828-942) showed no detectable beryl- lium. No beryl was observed in the granite in this area, and a chip sample of the granite (328-944) con- tained only 0.0008 percent BeQ. Along its northern and eastern boundaries the granite stock is in contact with Precambrian quartzite, and the southern boundary is largely covered by alluvium. The probability that - further search might reveal beryllium-bearing deposits along the granite boundary seems small. MONTANA By L. A. Warner and V. R. Wirararta Beryllium investigations in Montana were carried on during September 1949, in 18 districts and localities OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES (fig. 43). A variety of samples of igneous rocks and ore deposits was obtained. Principal attention was devoted to the Butte district, where helvite had been reported in rhodonite veins. The veins apparently do not contain enough helvite to make them a likely source of beryllium. A sample of tactite from the Mill Creek area, southwest of Anaconda, and a sample of mill tailings taken at the Drumlummon mine in the Marys- ville district contained 0.022 percent and 0.011 percent of BeO, respectively. There is no assurance that the samples are representative and further investigations at these localities are needed to determine the nature and quantity of the beryllium-bearing material. CASCADE AND JUDITH BASIN COUNTIES LITTLE BELT MOUNTAINS In the central part of the Little Belt Mountains, near Neihart, alkalic igneous rocks intrude limestones of Paleozoic age, and locally contact metasomatism has taken place. Metamorphosed limestone is exposed in a road cut on U. S. Highway 89, about 10 miles south of Neihart (fig. 44). The sedimentary rocks are part of the Barker formation of Weed (18992) (Cambrian) and consist of altered limestone, quartzsite, and shale. The igneous rocks are part of the group mapped by Weed as diabase, basalt, minette, vogesite, and kersan- tite. The igneous rocks exposed in the road cut include a lamprophyre dike and a light-colored aphanitic rock which may have been separately intruded or is an ex- tremely altered part of the lamprophyre. The lime- stone adjacent to the lamprophyre has been marmorized and partially replaced by silicate minerals. Taylor (1935) identified 27 minerals in the contact zone. A. grab sample (328-919) was taken from the contact zone on the east side of the road cut and a chip sample (328- 920) was taken across the altered limestone and shale exposed on the west side of the cut. Beryllium was not found in these samples; the lower limit of detection be- ing 0.0001 percent BeO. Yogo Peak is a prominent topographic feature in the Little Belt Range about 6 miles east of Neihart. It is formed by a Tertiary stock of shonkinite that cuts lime- stones, shales, and sandstones of Paleozoic age. Talus covers most of the contact on the west slope of Yogo Peak, and little or no metamorphism was found where the contact was exposed. On the east and northeast sides of the peak, massive limestone beds have been marmorized and locally replaced by garnet, actinolite, and diopside. A grab sample (328-921) of these con- tact minerals from a tactite zone, 3 miles by road north- east of the top of Yogo Peak, did 'not contain as much as 0.0001 percent BeQ. LOCALITIES IN MONTANA 110° 108° 106" 104° wee mee oue wen cm wk oor omni ae eh mein an enn ting chap me ahaa an hs [aad me iy saeco tae x= # ' hed i i 1 1 ‘ & | 1 ates I f $ --- | , sss Fi- * -J v- f Fl Glasgow } iad f i f f I ase! h - fl | 48° 2 7 & \ L‘p > H r r- 1 1 Sidney \ i i MISSOU RIVER \ 3 - _-" N i Jul SSV \\\ a I | l § L l _—-l'| t R 2 A I'M; L1 Er l L| t \| \ \ Jr; (Missoula l l + * ___1_—/ ‘ 1 < Ep eved a rode ie mares sinters \'\. -e 1 an way: - hie ---} A \ s _)] 17 W yt ~~ 1. { \ l a I re - --a f & A ) ".s-- ye. a" ' \ | ) : f -_E...a a “oi [l -- cam nl __ § on (uld ).2 F. o_ ---+} --' 1-2 3 x @: + 4s -3 f --r: i r y J“ | Billin *A C a meas sap! y 1" . (. | vas EXPLANATION = {J \ 1 Brogdus 1 ‘ el? F 4: LT gard H [J ¢ Locality sampled f ¥] C f 1 l 1____..__Z ___—-—-——l— TC" - \ ~! 7 114° 1 108° 106° Ed 0 200 Miles d 1409. 01 1-4 1 L 1 ld LOCALITIES Cascade and Judith Basin Counties Jefferson County Powell County 7. Basin district ; 1. Little Belt Mountains $; Elkhorn district ii 351135151; (Fight Deer Lodge County Lewis and Clark County sn £ C ¢ 2. Georgetown district 9. Marysville district ver Bow Lounty 3. Mill Creek area 10. Spring Hill mine g Ema? digitgicg '% Madison Count mey Granite County 11. Silver Star district d 17 voll Mountain aree 4. Garnet district 5. Philipsburg district Meagher County Sweet Grass County 6. Red Lion district 12. Gordon Butte 18. Haystack stock FIGURE 43.-Index map of Montana, showing localities sampled. DEER LODGE COUNTY CEORGETOWN DISTRICT - By W. T. Horser The Georgetown district is in the vicinity of George- town Lake, where U. S. Highway 10A crosses the sum- mit of the Flint Creek Range. It was sampled in June 1948 in connection with other geological work in the area. The geology of the district was described by Emmons and Calkins (1913, p. 221-242) and Holser (1950, p. 1063-1067). A stock of granodiorite 2 miles in diam- eter intrudes a faulted anticline of sedimentary rocks of Paleozoic age. Shaly limestones are metamorphosed to garnet-diopside and hornblende-magnetite tactites as far as 1,200 feet from the contact, and dolomite is re- crystallized and irregularly replaced by massive mag- netite near the stock. Later deposited pyrite, chalco- pyrite, pyrrhotite, arsenopyrite, and gold are wide- spread in the contact zone. The recrystallized and replaced limestones were sam- pled at several places along the northern edge of the stock as follows : 329-003 22-ft channel sample of magnetite-dolomite-olivine rock, from open pits of Pomeroy mine. 329-004 - 25-ft channel sample of dolomite marble partly altered to limonite, from opencuts on the Uncle Billy claim. 320-005 10-ft channel sample of dolomite marble at contact of granodiorite, from northeast crosscut of tunnel level, Cable mine. 150 820-006 10-ft channel sample of brecciated dolomite marble, from main tunnel near third crosscut, Cable mine. 15-ft channel sample of dolomite marble breccia and magnetite from tunnel level just north of Nowlan raise, Cable mine. 820-007 East side of rood cut 328 - 920 West side of rood cut 20 0 40 Feet Geology by L. A. Warner and V. R. Wilmarth, EXPLANATION September 1949 fom Talus Quartzite a Lamprophyre Sady shale Contact ~- 328-920 Locality sampled and number Altered limestone and shale FIGURE 44.-Sketches showing geology in road cut on U. S. Highway 89, in T. 12 N., R. 8 E., about 10 miles south of Neihart, Mont. Magnetite deposits near the contact of a granite stock at Olson Gulch (Holser, 1950, p. 1067, Emmons and Calkins, 1913, p. 244) were sampled as follows: 329-008 - 40-ft channel sample of magnetite-actinolite tactite in limestone, from northern open pits of the Bung- Your-Eye claim. 820-009 15-ft channel sample across a hematite-clay shear zone, same locality as sample 329-008. Beryllium was not detected in these samples, the lower limit of sensitivity being 0.001 percent BeO. MILL CREEK AREA Mill Creek rises in a valley that heads a short dis- tance west of Mount Haggin, a prominent peak about 80 miles southwest of Anaconda. The area is in the southeast part of the Philipsburg quadrangle, the geol- ogy of which was described by Emmons and Calkins (1913) and Calkins and Emmons (1915). The western , part of the quadrangle is underlain by rocks of the Belt series which in most places have been thrust over com- plexly folded and faulted formations of Paleozoic and Mesozoic age that lie to the east. The latter have been intruded by stocks, dikes, and sills ranging in composi- tion from granite to diabase. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES On the north side of Mill Creek, near its headwaters, shaly limestone in the Silver Hill formation of Cam- brian age has been contact metasomatized next to 2 granodiorite stock. A geologic sketch map of the con- tact zone exposed near the head of a northeast-trending gulch on the southeast side of Mount Haggin is shown in figure 45. 7 é dfleam Lake Creek. A mt. nace ,- Greek... 4, LJ Area of sketch 4 N. or! ’\% \ ae ANPC e +41 <+, Ax M“, a, \f 10 a 2 \%¢f (#" 3 xh. \. 49 1 0 2 Miles \./\ l {4 I J -~. 46° R. 12 W. 113° INDEX MAP TRUE NORTH ~ __| Granodiorite Mainly schist with some marble, pegmatite sills, .and granodiorite dikes Marble, shale, and biotite schist Marble Pegmatite sill Marble, shale, and biotite schist Pegmatite sill Marble "?y-Hornfels 2} Talus 200 0 400 Feet I SOL cani aly I 1 FIGURE 45.-Index and sketch maps of contact zone near Mount Haggin, Anaconda Range, Dear Lodge County, Mont. The rocks exposed in the contact zone are biotite schist, hornfels, marble, pegmatite sills, and narrow dikes of granodiorite. In places the marble and horn- fels have been replaced by idocrase and garnet. A composite sample (328-905) of idocrase-bearing rock from this locality contained 0.022 percent beryl- lium oxide. A mineralogical study of rock specimens from the contact zone was made by J. J. Glass, of the U. S. Geological Survey, in an effort to isolate and identify the beryllium-bearing mineral. The specimens were composed chiefly of idocrase, fluorite, calcite, bio- tite, spessartite, diopside-hedenbergite, hydrobiotite, LOCALITIES IN MONTANA quartz, and albite. The results of spectrographic analyses of these minerals for beryllium are shown in table 65. Taur 65.-Beryllia in minerals from contact zone, Mill Creek area, Montana [Qualitative spectrographic analyses by A. A. Chodes] BeO Description (percent) Idocrase from idocrase-fluorite-marble rock.______ 0.0X Fluorite from idocrase-fluorite-marble rock...... .O0X Calcite from idocrase-fluorite-marble rock__._... Not found. Biotite from idocrase-fluorite-marble rock___..... Not found. Garnet from quartz-feldspar-garnet rock____.--.-- Not found. Diopside-hedenbergite from hornfels____.. ___ .O0X Hydrobiotite from marble_______-------- __. .O00X Quartz and albite from veinlets_________-------- .OX Idocrase occurs chiefly in the relatively thin shaly limestone layers, in which it is an abundant constitu- ent. J. J. Glass of the U. S. Geological Survey made the following optical determinations on the idocrase : uniaxial negative; N.=1.700; N, (variable) 1.707 to 1.717; birefringence (variable) 0.007 to 0.015; dis- tinctly pleochroic in thick grains, colorless to yellowish green. A quartz-feldspar-garnet rock was found in float but was not observed in place. The garnet is spes- sartite (N=1.80 to 1.81) and is associated with micro- cline, albite, and quartz. Bands rich in diopside-hed- enbergite occur in hornfels near the pegmatite sills. Veinlets and stringers of quartz and albite presumably are related to the pegmatite. The contact zone in this area is extremely complex;, and detailed sampling would be needed as a basis for estimating tonnage. There is no assurance that the material collected at the locality visited is at all typical of the zone. Calking' map (Emmons and Calkins, 1918, pl. 1) shows the Silver Hill formation extending for more than 2 miles along the southern margin of the granodiorite stock in the vicinity of Mount Haggin. The mineral assemblage in the contact zone is one which commonly includes helvite, though none was found. GRANITE COUNTY By W. T. Hornser GARNET DISTRICT The Garnet district, including the Top 'Deep dis- trict, is along the crest of the Garnet Range, about 50 miles east of Missoula, and about 10 miles north of U. S. Highway 10. The area was visited in July 1948. The geology of the district has been described by Pardee (1917) and Holser (1950, p. 1067). A northwestward-trending anticline of limestones and shales of Paleozoic age is intruded by granodiorite of the Garnet batholith. Although recrystallization is widespread, contact metasomatism is confined to a nar- row zone near the granodiorite where shaly beds are 329-012 151 replaced by diopside, garnet, epidote, and magnetite. An eastward-trending fracture zone in the metamor- phic rocks contains local concentrations of quartz, barite, pyrite, tetrahedrite, chalcopyrite, galena, gold, telluride minerals, and molybdenite. A. 4-foot channel sample (329-014) was cut from a surface exposure of garnet-diopside tactite at the Sham- rock mine in the town of Garnet. At the Boston mine, a 15-foot channel sample (829-015) was taken across garnet and garnet-magnetite tactite in limestone. Spec- trographic analyses of these samples showed no beryl- lium, the limit of detection being 0.001 percent BeQ. PHILIPSBURG DISTRICT The Philipsburg district, which is on U. S. Highway 10A midway between Butte and Missoula, was visited in July 1948. The geology was studied by Emmons and Calkins (1913) and by Holser (1950). A northward- plunging anticline of sedimentary rocks of Paleozoic age is intruded by granodiorite of the Philipsburg batho- lith. Limestones are partly recrystallized, and shaly or sandy limestones are replaced by garnet-diopside tac- tite. Much of the tactite is replaced by magnetite, horn- blende, and scapolite. East-trending veins contain quartz, rhodochrosite, pyrite, galena, sphalerite, and argentiferous tetrahedrite; the oxide zones are rich in manganese. Samples were taken from the contact zone as follows (for localities see Holser, 1950, pl. 1) : 329-010 Channel sample across 15 ft of phlogopite-bearing marble, 235-ft level of Marie mine, 400 ft from shaft. 329-011 Channel sample across 20 ft of marble containing pyrolusite and quartz at headframe of True Fissure shaft. Channel sample across 15 ft of dolomite marble con- taining serpentine and magnetite, from end of south drift, main level, Climax mine. Beryllium was not detected in the samples, the lower limit of sensitivity being 0.001 percent BeQ. RED LION DISTRICT In the Red Lion district, about 10 miles southeast of Philipsburg, sedimentary rocks of Paleozoic age, mainly limestones, have been metamorphosed adjacent to the Philipsburg batholith. The metamorphism is less in- tense than in the Philipsburg and Georgetown districts nearby. Fracture fillings and replacement bodies in the limestone contain quartz, calcite, pyrite, hematite, mag- netite, and gold. A. prospect on the Modoc claim (Emmons and Cal- kins, 1913, p. 239) is on the contact between granodiorite and marble. Two channel samples were taken at this prospect, one (329-001) across 5 feet of granodiorite 152 and the other (329-002) across 12 feet of marble. The samples contain no beryllium, the lower limit of sensi- tivity being 0.001 percent BeQO. JEFFERSON COUNTY BASIN DISTRICT The Basin mining district, centering around the town of Basin, is about 8 miles west of Boulder and 20 miles south of Helena in the northern part of Jefferson County. The geology and ore deposits were described by Knopf (1913, p. 120-128) and Pardee and Schrader (1933, p. 285-299). The rocks exposed in the Basin dis- trict are quartz monzonite, dacite, and andesite of Late Cretaceous and Tertiary ago. The ore deposits include gold placers, and lodes that are valuable for silver, lead, zinc, and copper. Some composite lodes were worked chiefly for gold and silver. Samples were obtained at the Eva Mae and Hattie Ferguson mines. The Eva Mae mine and mill are 8 miles north of Basin. The country rock is quartz monzonite that has been cut by tourmaline-bearing quartz veins containing scheelite, galena, chalcopyrite, sphalerite, and pyrite. Grab samples of mill tailings (828-906) and ore from the mine dump (828-907) contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQ. The Hattie Ferguson mine is on Cataract Creek, about 6 miles north of Basin. The now abandoned mine was on a quartz vein in aplite. Galena, sphalerite, and auriferous pyrite are the principal ore minerals. A composite sample (328-908) of vein material from the dump contained no beryllium, the lower limit of sensi- tivity being 0.0001 percent BeQ. ELKHORN DISTRICT The Elkhorn mining district, centering around the town of Elkhorn, is about 12 miles northeast of Boulder, in the eastern part of Jefferson County. The geology and ore deposits were described by Weed (1901), Stone (1911), Knopf (1913, p. 128-139), and Pardee and Schrader (1983, p. 299-308). The sedimentary rocks are limestones, shales, and quartzites of Paleozoic age unconformably overlain by sandstones, shales, and im- pure limestones of Mesozoic age; all have been much altered by contact metamorphism. Tertiary andesite breccia, tuff, and lava overlie the sedimentary rocks of Mesozoic age. Intrusive igneous rocks of Cretaceous or Tertiary age range in composition from gabbro to granite. Samples were obtained from the Elkhorn and Sourdough mines and the Quartz Lode claim. The Elkhorn mine at the town of Elkhorn explores a lead-zinc-silver replacement deposit in indurated OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES limestone and shale. A composite grab sample (328- 909) of dump material contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQ. The Sourdough mine, a mile northwest of Elkhorn, is developed on a small pyrrhotite deposit in limestone near a quartz monzonite intrusive. Minor quantities of scapolite and epidote were noted on the dump. A grab sample (328-910) of dump material composed of epi- dote, scapolite, pyrrhotite, and limestone contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQO. A grab sample (828-911) of garnet from a small prospect pit on the Quartz Lode mining claim, one- fourth mile below the Sourdough mine, contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQO. LEWIS AND CLARK COUNTY MARYSVILLE DISTRICT The Marysville mining district is in Lewis and Clark County, about 17 miles northwest of Helena. The geology and ore deposits of the district were discussed by Barrell (1907), Knopf (1913, p. 61-76; 1950), and | Pardee and Schrader (1933, p. 63-76). The rocks of the Marysville district include a small quartz diorite stock that intrudes limestones and shales of the Belt series. Younger intrusive rocks are aplite, pegmatite, and diorite porphyry. The ore deposits are steeply dip- ping veins in the metamorphosed sedimentary rocks and the quartz diorite. Gold and silver are the prin- cipal metals produced. Only the Drumlummon mine (Clayton, 1888; Good- ale, 1915), on the north side of Marysville, was visited. The dump material consisted chiefly of indurated shales, marble, and hornfels, with very little garnet and epidote; the mine workings were inaccessible. A grab sample (328-913) of mill tailings from the Rainbow mill at the Drumlummon mine contained 0.011 percent BeOQ, A mineralogical study of this sample by J. J. Glass of the U. S. Geological Survey was undertaken to identify the beryllium-bearing mineral. The ma- terial was too fine for separation of individual mineral species; a magnetic fraction and three heavy mineral fractions were separated. The minerals recognized in the fraction with specific gravity greater than 3.3 are hematite, limonite, biotite, garnet, zoisite, epidote, and pyroxene. In the fraction with specific gravity between 2.8 and 8.3 chlorite, diopside, and carbonate were iden- tified. The fraction with specific gravity less than 2.8 contains chiefly quartz and feldspar. Magnetite is the chief constituent in the magnetic separation. The re- LOCALITIES IN MONTANA sults of spectrographic analysis for beryllium of the separate fractions are as follows: BeO Fraction (percent) Specific gravity >3.3 0. OOX Specific gravity >2.8<3.3 . OOX Specific gravity <2.8 . OOX Magnetic . OOX These analyses, though qualitative, cast some doubt upon the higher quantitative BeO value obtained for the bulk sample. No beryllium minerals were recog- nized in any of the fractions and the analyses suggest that the beryllium probably is dispersed in the various silicates. SPRING HILL MINE The Spring Hill mine is 4 miles southwest of Helena on the east side of Grizzly Gulch. The geology of the mine has been described by Knopf (1913, p. 101) and by Pardee and Schrader (1933, p. 207-209). The ore deposit is at the contact of a small body of diorite that intrudes Madison limestone (Mississippian). A dense gray-green rock composed of diopside and tremolite contains gold and some pyrite, pyrrhotite, and chlorite. In places, garnet, olivine, scapolite, sphene, and epidote replace the limestone. A grab sample (828-918) of ore and tactite minerals from the dump contained no beryl- lium, the lower limit of detection being 0.0001 percent BeO. MADISON COUNTY SILVER STAR DISTRICT The Silver Star mining district is northwest of the | town of Silver Star, about 25 miles airline southeast of Butte, in the northern part of Madison County. The geology and ore deposits of the district have been de- scribed by Winchell (1914, p. 189-144). The rocks ex- posed in this district are Tertiary granite, Cambrian (?) limestone, and Precambrian schist, slate, and quartzite. The limestone is metamorphosed and replaced by gar- net, epidote, magnetite, and pyrrhotite at its contact with granite. Gold, silver, copper, and lead occur in tactite deposits and a quartz vein. The Broadway mine, about 2 miles northwest of Silver Star, is on a tactite zone in the Cambrian limestone near the granite contact. A small glory hole exposes a U- shaped sulfide ore body composed mainly of gold-bear- ing pyrrhotite surrounded by tactite and hornfels con- taining magnetite, garnet, and epidote. The tactite zone extends northeast from the glory hole for about 700 feet, through two smaller opencuts, and southwest for about 500 feet. Ore deposition appears to have been controlled by a northeast-trending fault that approximately paral- lels the limestone-granite contact. A composite sample 467945-59--11 153 (328-896) of tactite from the workings and a grab sam- ple (328-897) of tailings from the mill contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQ. A grab sample (328-899) of garnet rock was collected from the dump of the Reconstruction Lode No. 3 mine, which is about 1 mile northwest of the Broadway mine. A quartz vein was mined for gold at this locality. The garnet contained no beryllium, the lower limit of sensi- tivity being 0.0001 percent BeQ. MEAGHER COUNTY GORDON BUTTE Gordon Butte, in the eastern part of Meagher County, is an eroded laccolith at the north end of the Crazy Mountains, geology of which was described by Wolff (1938). The rock composing the butte is theralite, an alkalic basalt containing augite, olivine, biotite, nephe- line, sodalite, and feldspar. A grab sample (328-922) of theralite from the north side of the butte contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQ. POWELL COUNTY OPHIR DISTRICT The Ophir mining district, centering around the aban- doned town of Ophir, is about 24 miles airline north- west of Helena in the eastern part of Powell County. The geology and ore deposits of the district were de- scribed by Pardee and Schrader (1933, p. 29-34). Lime- stones, shales, and quartzites of early Paleozoic age 0¢- cupy most of the area. East and west of Ophir are small masses of intrusive quartz monzonite of Tertiary age. The ore deposits are mainly gold and silver veins that are genetically related to the quartz monzonite. The sedimentary rocks have been partly altered to mar- ble, garnet tactite, and hornfels. The limestones ad- jacent to the intrusive bodies have been replaced by garnet, specularite, epidote, hornblende, diopside, cal- cite, tourmaline, sericite, and hematite. A composite sample (328-914) of tactite from the dump of the May- be mine near Ophir contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQ. PRIEST PASS AREA The road over Priest Pass, a short route across the Continental Divide from Helena to Blossburg, turns off U. S. Highway 10-N about 1 mile west of Spring Creek on the east side of MacDonald Pass. Near the top of Priest Pass, a prospect pit explores the contact of Ter- tiary quartz monzonite with the Quadrant quartzite (Pennsylvanian). A limestone layer in the quartzite has been partly replaced by brown garnet. A grab 154 sample (328-917) of garnet from the pit contained no beryllium, the lower limit of sensitivity being 0.0001 percent BeQ. SILVER BOW COUNTY BUTTE DISTRICT A brief visit was made to the Butte district to inves- tigate the occurrence of helvite reported by Hewett (1937) at the Lexington mine. According to Hewett, the helvite occurs as sparse lemon-yellow grains as much as 2 millimeters in diameter and as veinlets about 1 mil- limeter wide in rhodonite and rhodochrosite with minor amounts of galena, sphalerite, and pyrite. Through M. H. Gidel, chief geologist for the Ana- conda Copper Mining Co., permission was obtained to sample the Lexington mine. Helvite was noted in a mass of rhodonite as much as 3 feet wide and 30 feet long on the 200-foot level of the mine, 300 feet west of the shaft. A chip sample (328-902) taken across the rhodonite mass contained 0.00057 percent BeO. Similar rhodonite bodies have been found on the lower levels of the mine. They appear to be lenticular and to occur generally on the hanging wall of the vein. Analyses of composite grab samples from mine dumps in the Butte district are shown in table 66. Helvite was found in rhodonite on the dumps at the Moulton, Niagara, Alice, Magna Charta, and Lexing- ton mines. Rhodonite was virtually lacking in dump material at the Emma mine, rhodochrosite being the dominant gangue mineral, and no helvite was found. At all other dumps where samples were taken rhodonite was present and rhodochrosite rare or absent. The sample containing the most BeO (0.007 percent) was obtained at the Niagara mine where fluorite occurs in the gangue. Although analytical data on the BeO con- tent of the Butte ores are too meager for speculation, further sampling of rhodonite veins in which fluorite is a constituent may reveal local concentrations of helvite. It is doubtful that such occurrences would be large or of high grade, but in view of recent advances in flotation of nonmetallic minerals, recovery of helvite from rela- tively low-grade material may be possible in a large mining operation. TaBu® 66.-Beryllia in samples from mine dumps at Butte, Mont. Sample Mine (pg-33:15) 328-890 Lexington. Ll coe nn nee ele ol weld 0. 0016 891 Moulton. . £.. - 2e 22 6022 n an a a eau a eee waw. . 0023 801A :! ° / 'do. score lille incl itty POOL . 0015 892 Alico. csc olson. . 0042 893 Magna Charta..-..............s.s.... . 0030 894 .. si ttl _o saum [00 n. d. ! 903 Alice (vein outcrop, east of shaft) _____. . 0005 904 Minagara s J 2. .l ine nna Ab . 0070 * Not detected, lower limit of sensitivity being 0.0001 percent. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES In the course of sampling the mines of the Anaconda Copper Mining Co. at Butte a visit was made to the company's smelter at Anaconda. Company officials kindly provided samples of the mill and smelter prod- ucts of ores from several localities Twelve of the samples were selected for spectrographic analysis and are described in table 67. In connection with the Mine, Mill, and Smelter Survey, 12 samples of mill and smelter products were obtained in 1945 from the Washoe Reduction Works at Anaconda. The ores treated were from various mines in the Butte district. Analytical data for these samples are given in table 67. Results of analyses indicate that very little beryl- lium is contained in the ore minerals at Butte. Pre- sumably most of it occurs in helvite associated with the gangue and is lost in beneficiating the ore. 67.-Beryllia in samples from Washoe Reduction Works, Anaconda, Mont. [nd not detected; lower limit of sensitivity is 0.0001 percent BeO. Samples 310- ACM-1 to -20 collected in 1945 by Mine, Mill, and Smelter Survey and analyzed by K. J. Murata and E. W. Claffey] peo e Sample Description (percent) 328-952 Third shift, Sept. 1, 1949, Agitair tails, Butte Copper ore___L____________ nd 963 Final tails bulk float, zinc ores, Butte, MONb: - m rew sr. - 2 en bea ah at an a 0. 0004 966 Third shift, Aug. 15, 1949, manganese COnCEBIMATE.: .- nd 973 Lot No. B-64, copper concentrate, Cooke 'City, el .s nd 974 Lot No. 981, waste slag ferroman- SMICSG. . -==- *see a- «a . 0001 975 Second shift, Aug. 28, 1949, man- cee eevee li . 0001 975A Conda phosphate footwall rock...... . 0004 975B Conda phosphate hanging-wall rock.. nd 977 Lot No. FM-7, ferromanganese metal.. nd 981 Black sand, Rock Creek district, 2 cel sn nn be aa inn sare ane a nd 988 Third shift, Sept. 1, 1949, Agitair concentrate, Butte Copper ores.... nd 989 Zinc concentrates, Butte ores_______. nd 310-ACM-1 Sulfide concentrate, Emma mine (Pb- Zn-Ag ore, rhodochrosite gangue) ... _ 0002 ACM-2 Sulfide tailings, Emma mine__._.___. 0002 ACM-3 Copper flotation tailings, Butte mines. 0002 ACM-4 Copper concentrate, Butte mines.____. nd ACM-5 Arsenic roaster residue, Butte mines.. 0002 ACM-6 Granulated reverberatory slag (copper), Butte MMHCS. .. . . Cee cu . 0002 ACM-8 Iron table concentrates, Butte mines.. nd ACM-9 Flue dust (copper), Butte mines.... nd ACM-17 - Zinc concentrates, Butte mines.______ nd ACM-18 - Lead concentrates, Butte mines_______ nd ACM-19 _ Zinc-lead tailings, Butte mines... 0008 ACM-20 - Zinc concentrates, Butte mines._._.____ nd HIGHLAND DISTRICT The Highland district is in the southern part of Silver Bow County, about 25 miles south of Butte. Ac- cording to Winchell (1914, p. 87-90), the rocks of this district consist of a series of slates and quartzites of Belti age underlying a thick limestone bed, probably Paleozoic in age, all of which are intruded by quartz monzonite, diorite, granite, and aplite, presumably of Tertiary age. Garnet, epidote, magnetite, diopside, and LOCALITIES IN WYOMING actinolite replace the limestone at its contacts with igneous rocks. The Highland mine, at the head of the main fork of Fish Creek, is on the north side of a large limestone inclusion or roof pendant in granite. The ore body has been described by Newcomb (1941). The ore is chiefly pyrrhotite, pyrite, and chalcopyrite, in a gangue of coarsely crystalline tremolite, epidote, and diopside. A composite grab sample (328-901) from the dump contained less than 0.0001 percent BeQ. Approximately 2 miles west of the Highland mine is a tactite zone 50 feet wide and several hundred feet long in the limestone. A composite grab sample (328- 900) of garnet, diopside, magnetite, and epidote from the tactite zone did not contain as much as 0.0001 per- cent BeQ. TOLL MOUNTAIN AREA Toll Mountain is 19 miles southeast of Butte near the boundary between Silver Bow and Jefferson Counties. At this locality, sedimentary rocks of Paleozoic age consisting of slate, marble, and quartzite appear to form a roof pendant in a Tertiary intrusive granite body. The sedimentary rocks strike N. 45° E. and dip steeply northwest. A garnet tactite zone can be traced north- east for several hundred feet along the contact between granite and marble, beginning at an outcrop about 800 feet north of the Toll Mountain Ranger Station. The garnet zone locally contains thin lenses of diopside. The granite adjacent to the sedimentary rocks has been endomorphosed. A composite grab sample (828-895) of the garnet rock did not contain as much as 0.0001 percent BeQO. SWEET GRASS COUNTY HAYSTACK STOCK Haystack stock, about 55 miles south of Big Timber, is 1 mile south of the old mining camp of Independence in Sweet Grass County. The geology has been de- scribed in detail by Emmons (1908). We made a brief visit to the area to sample the contact zone on the west side of the stock. The intrusive body, according to Emmons, ranges in composition from quartz monzonite to olivine gabbro and extends from Haystack Peak to Baboon Mountain, a distance of 3 miles. Limestones, shales, and sandstones of Cambrian age have been meta- morphosed and replaced by tactite at the contact with the intrusive rock. Garnet, epidote, quartz, and actino- lite are the principal tactite minerals. A composite grab sample (328-923) of tactite from the contact zone did not contain as much as 0.0001 percent BeQ. 155 WYOMING By L. A. Warner and V. R. Beryllium investigations at 15 localities in Wyoming (fig. 46) were made during October 1948 and August 1949. The BeO content of 31 samples selected for spectrographic analysis ranged from less than 0.0001 percent to 0.003 percent. The samples represent many types of nonpegmatite rocks and mineral deposits. Present information does not appear to warrant further sampling at any of the localities. ALBANY COUNTY CENTENNIAL DISTRICT The Centennial district centers around the town of Centennial in the eastern part of the Medicine Bow quadrangle. The geology of the area was described briefly by Darton and Siebenthal (1909, p. 49-50). The ore deposits consist of gold-bearing quartz veins in Pre- cambrian schist, gneiss, and granite. Samples were collected from two mines, the Utopia and the Inde- pendence. The Utopia mine is 1 mile northwest of Centennial on the east side of Centennial Ridge. Gold is found in a 3-foot wide, west-trending quartz vein in hornblende schist. Additional vein materials are calcite, pyrite, sericite, limonite, and garnet. A composite sample (328-9877) of dump material showed no beryllium, the limit of sensitivity being 0.0001 percent BeQ. The Independence mine is 2 miles west of the Utopia mine on the west side of Centennial Ridge. The mine is developed on eight narrow pegmatite stringers in hornblende schist. A 6-foot channel sample (828-878) across the back of the adit, 10 feet from the portal. did not contain as much as 0.0001 percent BeQO. IRON MOUNTAIN Iron Mountain is on the eastern flank of the Laramie Mountains in sees. 22, 23, and 27, T. 19 N., R. 71 W., 'about 40 miles northeast of Laramie. Geology of the area has been described by Diemer (1941, p. 6-11), and is shown on figure 47. A north-trending dikelike body of titaniferous magnetite 50 to 350 feet wide can be traced for nearly a mile. The adjacent rock is Pre- cambrian anorthosite with some gabbro. Near the center of the ore body, a small plug of granite cuts the magnetite and anorthosite. The anorthosite and gab- bro are fractured and hydrothermally altered on either side of the ore body at its southern end, where the con- tacts are exposed on Chugwater Creek. 156 110° 108° OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 106°. 104° -- in to 7“'—"'T"—" OSheridan Ge--- | EXPLANATION ©14 Locality sampled for this report 44° 44 Calan mesa 42° 42° ____<’.__--.____.-..T__-___- O Rock Springs ALBANY COUNTY . Iron Mountain . Rambler mine . Strong mine th G0 Do - CARBON COUNTY . Hanna district . Rawlins area ngo Samples were taken as follows (see fig. 47 for lo- cations) : . Centennial district . Encampment district 106° 104° 12IO'Miles PLATTE COUNTY 12. Halleck Creek area 13. Welcome mine FREMONT COUNTY 8. Fort Washakie area LARAMIE COUNTY 9. Silver Crown district NATRONA COUNTY SWEETWATER COUNTY 14. Leucite Hills 15. Superior district 10. Casper Mountain 11. Garfield Peak FicurE 46.-Index map of Wyoming, showing localities sampled. 210 Chip sample across magnetite body at top of Iron Mountain. 212 Grab sample from outcrop of granite plug. 828-206 Chip sample across 25 ft of gabbroic anorthosite with some magnetite. 207 Chip sample across 30 ft of altered anorthosite and gabbro. 209 Chip sample across 6-ft gabbro dike. Spectrographic analyses showed no beryllium in the samples, the limit of detection being 0.001 percent BeQO. LOCALITIES IN WYOMING TRUE NORTH EXPLANATION XAX eines XXX 7 a XC wea ps 7 IA \ Granite < " ~A. -/, la "~ U ..}. / /Y s- Pol L4 1T -. / c " >- BSS 1 ~ \,_ / Besa '.~ % \ eod 1 . Cd 70 c - ) /. - | «7. ,-- en ? LAY. ; \ Includes some gabbro ASS: é gy :'> /" X l/ 'a ~ -‘ b o $> r \' By) /\ > Contact - PSR /c \ T,C 2. TRY 1. -! B - ars-200 a BSI ¥ Locality sampled and number e Cot late R C O " and number h , ) Pate! ”75:55: rormalels fested "67:55:90 Hamels Geology by L. A. Warner and V. R. Wilmarth, September 1948 500 0 500 Feet 40 0 40 Feet FigurB 54.-Geologic sketch maps of parts of Italian Mountain area, Gunnison County, Colo. LOCALITIES IN COLORADO of Gunnison County. The geology of the Italian Moun- tain area was described by Emmons, Cross, and Eld- ridge (1894, p. 5) and by Cross and Shannon (1927). North and South Italian peaks are formed by masses of intrusive rock that range in composition from diorite to granite. - Sedimentary rocks of the Weber formation (Pennsylvanian) crop out on the flanks of North and South Italian Peaks, and form Italian Peak. Near their contacts with intrusive bodies the sedimentary rocks have been metamorphosed and replaced locally by tactite (fig. 54). Shannon (in Cross and Shannon, 1927, p. 9) described 28 minerals from the tactite zones. A wedge-shaped body of limestone, shale, and sand- stone in the Weber is exposed on the west flank of Ital- ian Peak between the northern and southern intrusive masses. -A limestone bed has been replaced by a tactite layer 15 feet thick containing brown and yellow grossu- larite-andradite garnet, actinolite, sphene, idocrase, magnetite, and epidote. Southwest of North Italian Peak is a smaller wedge-shaped mass of intensely al- tered Weber formation consisting of interlayered quartzite, hornfels, marble, tactite, and some graphite. 'Ten samples were taken as follows (see also fig. 54) : 328-078 Grab sample of marble containing epidote, garnet, and diopside, North Italian Peak. Do. Grab sample of tactite containing garnet, diopside, and actinolite, Italian Peak. Grab sample of tactite containing garnet, diopside, and epidote, Italian Peak. Grab sample of garnet tactite float, Italian Peak. Grab sample of epidote tactite float, Italian Peak. Chip sample across 6 ft of silicated marble contain- ing magnetite, phlogopite, garnet, and actinolite, North Italian Peak. Chip sample across 12 ft of garnet tactite, North Ital- ian Peak. Chip sample across 25 ft of quartzite with thin layers of hornfels, North Italian Peak. Chip sample across 100 ft of gilicated limestone and hornfels containing tremolite and garnet, Italian Peak. No sample contained as much as 0.001 percent BeQO. 079 080 081 082 083 682 683 684 689 SNOWMASS MOUNTAIN AREA The Snowmass Mountain area is in the Elk Moun- tains in the extreme northern part of Gunnison County. The geology and mineral deposits were described by Vanderwilt (1937). Sedimentary rocks ranging in age from Cambrian to Cretaceous have been metamor- phosed for several thousand feet outward from their contact with a Tertiary albite granite mass that forms Treasury Mountain. Zinc, lead, and silver are the major metals produced from quartz veins in faulted sedimentary rocks. In the area at the head of Yule Creek (fig. 55) garnet 171 tactite bodies as much as 25 feet thick occur near the top of the Leadville limestone (Mississippian). Thin bands of epidote, garnet, diopside, and quartz replace lime- stone layers in the Hermosa group (Pennsylvanian). ~~ ~f j." / semen 328-086, 087 Geology by L. A. Warner and 328-084 , 085 TA V. R. Wilmarth, September 1948 % { Mooo 'd 1000 Feet % EXPLANATION 2s % £2 a . + #9 Contact, showing dip Dakota sandstone } 9° Dashed where approximately located p A Hermosa group J&S | ui Strike and dip of beds is .% (Z s £2 & s2s-o88 Leadville limestone | $5; | S Sample number a 8 nix [=a Ces a Ga Fieurs 55.-Geologic sketch map of tactite zone near head of Yule Creek, Snowmass Mountain area, Gunnison County, Colo. Five samples from the tactite layers in this area were taken, as shown on figure 55, and are described below. 328-084 Grab sample of garnet-bearing rock from north side of tactite zone. Same, from south side of tactite zone. Chip sample across 25 ft of garnet tactite. Chip sample along outcrop of tactite layer for 200 ft. Grab sample from outcrop of garnet tactite layer. 085 086 087 088 None of the samples contained as much as 0.001 per- cent BeQO. In the Rock Creek area, near Schofield Pass 12 miles northwest of Gothic, quartz veins containing pyrite, epidote, specularite, tourmaline, galena, and sphalerite occur along north-trending faults. A chip sample (328-692) across a 10-foot-wide quartz vein contained less than 0.0001 percent BeQO, if any. The Niobrara limestone (Cretaceous) has been replaced by garnet, epidote, calcite, diopside, and actinolite at the contact 172 of a Tertiary lamprophyre dike. Two channel sam- ples (3828-693 and -695) across altered limestone ad- jacent to the dike showed no BeQO. TINCUP DISTRICT The Tincup district is in the Sawatch Range, a few miles south and southeast of the village of Tincup. The formations include Precambrian granite gneiss and sedimentary rocks of Paleozoic age, chiefly limestone, ranging in age from Cambrian to Pennsylvanian. Ter- tiary quartz monzonite sills, dikes, and small stocks cut the sedimentary rocks. The sedimentary formations trend northwesterly and dip 10°-85° NE. The ore deposits of the district are of four types (Goddard, 1936, p. 565) ; silver-lead-gold blanket de- posits, silver-lead-gold veins, molybdenum-tungsten veins, and pyrometasomatic iron deposits. The silver- lead-gold deposits account for most of the production. The blanket deposits and pyrometasomatic deposits are in limestone; the veins cut all rock but were most pro- ductive in limestone. Several mines in the district were visited, and the samples taken are described in table 71. TaBu® 71.-Beryllia in samples from the Tincup district € Sample Descripti on ( plearcgnt) 328-669 Grab sample from 2-ft quartz vein con- taining huebnerite, molybdenite, pyrite, chalcopyrite, sphalerite, and galena, Ida May mine, 5 miles south of Tincup at Cumberland _ Channel sample across 3-ft quartz vein containing molybdenite and pyrite, Emma H mine, 1 mile west of Cumber- land Pages 2 cule. .ro nle ls Grab sample from 6-ft quartz vein contain- ing molybdenite at Mammoth mine, 3 mile west of Ida May mine...... Grab sample containing galena, pyrite, chalcopyrite, limonite, and quartz from dump of Jimmy Mack mine, 5 miles south.of .I.: Channel sample across 6-ft zone of garnet tactite, Cumberland mine opencut on Gold Hill, 4 miles south of Tincup..__._. Channel sample across 10-ft layer of mag- netite containing some garnet, Cumber- land ceta lll" Channel sample across altered quartz mon- zonite sill, Cumberland opencut.______ Grab sample containing molybdenite, pyrite, and quartz from dump of Bon 1'I)‘on mine, 3 miles south of Cumberland AES L n een ore ee ce nas ae ain an aids ane s. o ole <0. 0001 670 . 0013 671 <. 0001 673 <. 0001 675 <. 0001 676 <. 0001 <. 0001 677 681 . 0005 TOMICHI DISTRICT The Tomichi, or Whitepine, mining district is in the eastern part of Gunnison County on the west slope of the Sawatch Range. Most of the mines are east and north of the mining camp of Whitepine. The geology and ore deposite of the district were described by Harder (1909, p. 194-198), and Crawford (1913, p. 284- 310). Sedimentary rocks ranging in age from Ordo- vician to Pennsylvanian are in fault contact on the east OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES with Precambrian granite and are bounded on the west by Princeton quartz monzonite of Crawford (1913) of Tertiary age. The ore deposits are replacement bodies in limestone and dolomite, contact deposits, and fissure veins. The principal metals produced are lead, zinc, and silver. Contact deposits and veins near the Iron King mine, northeast of Whitepine, were sampled (fig. 56). EXPLANATION SEDIMENTARY ROCKS Sacto TERTIARY ._ Belden shale Stippled where altered IGNEOUS ROCKS EYS yr As" sta Princeton quartz monzonite of Crawford (1913) Tave Nort RON KING MINE Souls PRECAN TERTIARY BRIAN = In | Granite Contact - Dashed where approximately located & &/ 1 ¢ I/ Strike and dip of beds It hs /// Magnetite ore [a Vertical shaft > Adit 2 X (3) Prospect pit MORNING GLIM VEIN 328-029 K5 r-328-029 \» _ Locality sampled and number Geology by L. A. Warner and V. R. Wilmarth, 500 (I) j IOPO Feet 1949 FIGURE 56.-Geologic sketch map of part of northern Tomichi district, Gunnison County, Colo. The samples collected in the Tomichi district (See fig. 56 for some localities) are listed below. None showed as much as 0.0001 percent BeQ. 328-022 8 ft channel sample across tactite on hanging wall of magnetite body. 023 Chip sample across silicified limestone between mag- netite zones. 024 Grab sample of magnetite. 025 Grab sample of epidote, garnet, and silicified lime- stone. 026 Grab sample of silicified limestone. 027 Grab sample of silicified limestone with garnet, epi- dote, and magnetite. 028 Grab sample of limonite-stained silicified limestone. 029 Grab sample of sulfide ore from vein. 030 Grab sample of altered shale and limestone contain- ing magnetite. 031 Grab sample of epidote-garnet rock from dump of Erie mine. 033 Grab sample of tailings from Callahan Zinc-Lead Co. mill at Whitepine. 033A ' Grab sample of mill heads from Callahan Zinc-Lead Co. mill at Whitepine. 033B - Garnet-epidote rock from level 4, Erie mine. 0330 - Garnet-epidote, galena, and sphalerite, main drift, Erie mine. 033D Galena and sphalerite from main drift, Erie mine. 033E - Ore from main drift, Erie mine. The Iron King mine is about 2 miles by road north- west of Whitepine near the Morning Glim fault. Mag- LOCALITIES IN COLORADO netite ore in a zone 65 feet wide extends along the fault for several hundred feet. Masses of serpentine and quartzite interlayed with magnetite are exposed at the Tron King opencut. Adjacent to a quartz monzonite dike the limestone and shaly layers of the Belden shale have been heavily impregnated with epidote, chlorite, actinolite, garnet, pyrite, and magnetite. Tactite min- erals partly replace the shaly layers of the Belden shale near the Parole tunnel. Samples of tactite from the underground workings of the Erie mine at Whitepine were obtained through the courtesy of C. S. Robinson of the TU. S. Geological Sur- vey. Samples of mill products were obtained from the Callahan Zinc-Lead Co. mill at Whitepine. HINSDALE COUNTY LAKE CITY DISTRICT The mining district near Lake City, in the western part of Hinsdale County, includes two major mining camps: Galena (Henson Creek) camp west of Lake City along Henson Creek and the Lake Fork camp at the north end of Lake San Cristobal about 5 miles south of Lake City. The geology and ore deposits of the Lake City district have been described by Irving and Ban- croft (1911), Brown (1926), and Burbank (in Vander- wilt, 1947, p. 439-443). ; 'The rocks of the district are mainly of the Silverton volcanic series of Tertiary age. Intrusive bodies of rhyolite, latite, and quartz monzonite in places cut the volcanic rocks. The ore deposits are chiefly fissure veins containing lead-zine ores and a little gold, silver, and copper. The principal gangue minerals are rhodo- chrosite, quartz, and barite. The veins in the Lake City district are similar to hel- vite-bearing veins in the Eureka area nearby, except that the latter contain rhodonite. Samples obtained at seven mines in the district are described in table T2. No helvite was noted in any of the veins. Tasos 72.-Beryllia in samples from the Lake City district B Description (perieont) Grab ~ sample containing rhodochrosite, quartz, galena, sphalerite, and altered rhyolite from dump of Ulay tunnel, on Iélfinson Creek 3.5 miles west of Lake iY o ews aes nases Grab sample of ore from dump of Hidden Treasure mine, 2,000 ft northwest of TUlay tunnel (tetrahedrite, galena, sphal- erite, quartz, rhodochrosite, and jasper) -- Grab sample containing tetrahedrite, galena, sphalerite, pyrite, chalcopyrite, and quartz from dump of Wave of the Ocean mine, on Henson Creek 7 miles west of Lake City. Grab sample of ore from bunker at Yellow Medicine mine, 2 miles northeast of Capi- tol City in Yellowstone Gulch (galena, sphalerite, chalcopyrite, and quartz). - Sample 328-573 0. 0002 576 <. 0001 579 . 0002 580 <. 0001 1783 Tasos 69.-Beryllia in samples from the Lake City district-Con. BeO Sample (percent) 581 Description Grab sample of lead-zine ore from dump of Capitol mine, one-quarter mile southwest of Yellow Medicine mine.__----.-------- 586 Grab sample of ore from dump of Golden Fleece mine, 1,200 ft west of north end of Lake San Cristobal (galena, pyrite, and gold telluride, with rhodochrosite and 588 Grab sample containing galena, pyrite, sphalerite, and quarts from dump of eneral Sherman mine, in Slumgullion Gulch 1 mile north of Lake San Cristobal. <0. 0003 <. 0003 <. 0001 HUERFANO COUNTY WALSENBURG AREA By W. T. HorsEr Near Walsenburg, flat-lying Cretaceous and Tertiary sedimentary rocks are cut by small intrusive bodies that are probably related to the Tertiary igneous com- plex of the Spanish Peaks to the southwest. The prin- cipal bodies are northeasterly trending vertical dikes several miles long and as much as 50 feet thick; they range in composition from basalt to granite. There are a few sills and plugs. Details of the geology were de- scribed by Hills (1900). One of the plugs forms Huerfano Butte, on the east side of U. S. Highway 85-87 and south of Huerfano Creek (Knopf, 1936, p. 1776). The rock is an alkali gabbro composed mainly of labradorite, augite, biotite, olivine, and potassium feldspar. A sample (329-251) from the top of the butte on the north side contained 0.002 percent BeOQ. An olivine basalt dike containing titanaugite crosses the highway about 3 miles south of Huerfano Butte. A 12-foot channel sample across the dike contained 0.0008 percent BeQO. Seventeen samples of various rocks collected by Knopf were analyzed chemically and also were tested spectro- graphically for beryllium with negative results, the limit of sensitivity being 0.0X percent (Knopf, 1936, p. 1779) . Although the beryllium contents of the samples from the Walsenburg area are much too low to be of com- mercial interest, the 0.002 percent BeQO in gabbro at Huerfano Butte is considerably above the average for mafic rocks. Theoretically, some of the silicie and al- kalic rocks in the Spanish Peaks region might be ex- pected to contain appreciably more beryllium. LAKE COUNTY CLIMAX MINE Ten samples of mill products furnished to the Geo- logical Survey by the Climax Molybdenum Co. in 1950 were analyzed for BeQ. Descriptions of the samples and analytical results are given in table 78. Details 174 of the geology of the Climax mine are given by Butler and Vanderwilt (1933). TaBus 73.-Beryllia in samples of mill products from Climax, Colo. B Sample Description (”fun CMC 1 Molybdenite concentrate______________ <0. 0001 1A : Quarts tailings....". __ . 0005 8 Huebnerite .._ __ . 0004 4 Quarts tailings . 0005 6 Eyrite concentrate.:.: L <. 0001 7 Huebnerite concentrate.___._._._________ <. 0001 8 Topaz <. 0003 12 Monazite concentrate... _____._______._ <. 0003 14 Cassiterite concentrate. _ _________.____ . 0005 762 Molybdenite mill heads_._.._.._._____ ___ 0006 LA PLATA COUNTY DURANGO AREA Coals of Late Cretaceous age occur in the Durango area, principally in the Mesaverde and Fruitland formations. The deposits have been described by Gardner (1909). Samples were obtained from the Castle, 0. K., and Yellow Jacket coal mines and from coal outcrops east of Durango. Ash from a grab sample ( 328-158) of coal from the Castle mine, 5 miles northwest of Durango, contained 0.0003 percent beryllium, 0.006 percent germanium, 0.004 percent gallium, and 0.02 percent vanadium. Ash of coal (328-163) from the Yellow Jacket mine, east of Bayfield on U. S. Highway 160, contained 0.0008 percent beryllium, 0.005 percent gallium, and 0.008 percent vanadium. LAS ANIMAS COUNTY MORLEY AREA By W. T. HorsEr T wo mafic dikes are exposed in a road cut on the east side of U. S. Highway 85-87 at Morley station, a few miles north of the New Mexico State line. The rock is greenish black, fine grained, and rich in augite. A 6-foot channel sample (829-254) across the northern dike showed no BeO ; the limit of sensitivity for the spectrographic analysis was 0.0004 percent. An intrusive body of basalt about half a mile in di- ameter crops out 2 miles east of Morley. The rock con- sists of augite and olivine phenocrysts in a groundmass of plagioclase, augite, and magnetite (Hills, 1899, p. 3). At the southwestern margin of the intrusive, the rock is light gray and probably more silicic than basaltic. A sample (329-257) of this rock showed no beryllium, the limit of sensitivity being 0.0004 percent BeQ. MINERAL COUNTY CREEDE DISTRICT The Creede district is near the eastern edge of the San Juan Mountains in the northern part of Mineral OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES County. The principal mines are a few miles north- east of the town of Creede. The geology and ore de- posits of the district were were discussed by Emmons and Larsen (1923). The ore deposits are silver-lead veins in Tertiary rhyolite and in quartz latite flows. The principal ore minerals are galena, pyrite, chal- copyrite, and sphalerite in a gangue of amethyst, quartz, chlorite, and fluorite. Samples of the mill products were obtained at the Emperius Mill in Creede. Analyses of both mill heads and mill tails (samples 328-591, -592) showed 0.002 percent BeQ. WAGON WHEEL GAP Fluorspar veins occur in Miocene rhyolite tuffs and breccias about 1 mile south of Wagon Wheel Gap sta- tion on the Denver and Rio Grande Western Railroad. The geology and ore deposits of the area were de- scribed by Aurand (1920, p. 61-67 ) and Emmons and Larsen (1913). The main deposit is on the east side of Goose Creek, across the valley from Mineral Hot Springs. It is owned and operated by the Colorado Fuel and Iron Corp. at Pueblo. A grab sample (328- 598) of white fluorite from the ore bin contained no beryllium. MONTEZUMA COUNTY RUSH BASIN Rush Basin is a large erosional valley at the head of the East Mancos River in the La Plata mining district. A description of the geology of the area is given in a comprehensive report on the La Plata district by Eckel, Williams, and Galbraith (1949, p. 110-115). Many dikes, sills, and small stocks of diorite monzonite, and syenite porphyry cut metamorphosed sedimentary rocks of Jurassic and Cretaceous age. Several mines in the area exploit gold-bearing breccia deposits, blanket or replacement deposits, and fissure veins. A 1-foot-wide tactite zone composed of brown garnet, epidote, actino- lite, calcite, quartz, and a minor amount of pyrite is exposed about 700 feet N. 80° E. of a cabin at the en- trance to Rush Basin. The tactite zone is in a limestone member of the Wanakah formation of Jurassic age. A grab sample (828-155) of the tactite showed no bery]- lium, the limit of sensitivity being 0:0001 percent BeQ. oURAY COUNTY OURAY DISTRICT The Ouray district centers around the town of Ouray in the San Juan Mountains of southwestern Colorado. The geology and ore deposits of the Ouray district have been described by Irving (1905) ; Cross, Howe, and Irving (1907) ; and Burbank (1930; 1940). The rocks exposed in the Ouray district include 8,000 feet of Pre- LOCALITIES IN COLORADO cambrian quartzites and slates and about 5,000 feet of limestones, shales, and sandstones of Paleozoic and Mesozoic ages. Unconformably overlying the strata of Mesozoic age is a thick series of Tertiary volcanic rocks, consisting chiefly of andesite flows and latite tuff and breccia. The principal ore deposits occur in strata of Paleozoic and Mesozoic age near Tertiary granodiorite and quartz monzonite porphyry intrusive bodies. Py- rometasomatic deposits, fissure veins, and flat-lying re- placement deposits are represented. Beryllium was not detected spectrographically in any of the samples, the limit of detection being 0.001 percent BeQ. These are samples collected in the district: 328-119 Grab sample containing chalcopyrite, pyrite, diopside, epidote, and quartz from dump of Bright Diamond mine, 1 mile north of Ouray. Channel sample across 8-ft tactite zone at portal of Bright Diamond adit, 500 ft southeast of Bright Diamond mine. (Tactite is chiefly garnet, epidote, actinolite, and chlorite; ore minerals are pyrite, chalcopyrite, galena, sphalerite, and magnetite.) Grab sample from dump of Portland mine, 1.5 miles east of Ouray (calcite, siderite, rhodochrosite, and quartz, with minor amounts of galena and sphale- rite). Mill heads, American Zinc, Lead, and. Smelting Co. mill at Ouray. Mill tails from same place. 120 123 861 862 RED MOUNTAIN DISTRICT 'The Red Mountain district is along Red Mountain Creek in the southern part of Ouray County, between Tronton Park on the north and Red Mountain on the south. The geology and mineral deposits have been de- scribed by Ransome (1901b, p. 214-250) , Collins (1931), and Burbank (in Vanderwilt, 1947, p. 428-481). The Tasun 74. -Berylli a in samples from the Red Mountain district BeO (percent) Sample Description 328-127 Grab sample of altered volcanic rock con- taining galena and sphalerite from dump of Mountain King mine, 2 miles north- east of Red Mountain 0. 0004 Chip sample across 125 ft of silicified vol- canic material near ore bin at Guston mine, 1.5 miles north of Red Mountain -:... .l. cls oo ae Composite grab sample of silicified vol- canic material from dump of Guston HMG. L .._ GEL .W sens Chip sample across southwest end of silic- ified pipe at National Belle mine at Red Mountain Pass._-_------.----------- Grab sample of sericitized volcanic rock at southwest end of shaft house, National Belle mine."... o Chip sample across northeast end of silic- ified pipe, National Belle mine.__.-.--.. Mill heads from Idorado mill at Treasury Tunnel, 1 mile north of Red Mountain PASK- ".. «cadence can news' -a Mill tails from Idorado mill___---------- 128 . O01 130 001 132 001 134 001 001 137 859 . 0001 . 0001 AA cA AGX X B 860 175 Silverton volcanic series of Tertiary ago several thou- sand feet thick, constitutes the major part of the ex- posed bed rock. These rocks are intruded by porphy- ritic latite and rhyolite plugs that range from a fow feet to more than 2,000 feet in diameter. Much frac- turing accompanied intrusion, and the volcanic rocks were altered to clay minerals, alunite, diaspore, and quartz along vertical pipelike zones. Ore deposits con- taining sulfides of copper, silver, lead, and zinc are associated with the siliceous pipes. Samples collected in the district are described in table 74; none contained as much as 0.001 percent BeQ. UPPER UNCOMPAHGRE DISTRICT The Upper Uncompahgre district includes the mines along Uncompahgre Canyon, and along Red Mountain Creek between Ironton Park and the junction with Un- compahgre River. The geology and mineral deposits were described by Burbank (in Vanderwilt, 1947, p. 437-439), and Kelley (1946, p. 355-385). The rocks in Uncompahgre Canyon are Precambrian quartzites and slates that are uncomformably overlain by sand- stones, shales, conglomerates, and limestones of Devo- nian to Jurassic age. Tertiary volcanic tuff, breccia, andesite, and latite, of the Silverton volcanic series and the San Juan tuff, overlie the older rocks. Prevolcanic intrusive rocks consist of quartz monzonite and diabase dikes. The ore deposits in this area are vein and chim- ney deposits in the altered volcanics. Two types of vein deposits are found: pyrite-gold-quartz, and tung- sten-quartz. Chimney deposits are characterized by lead, zinc, and copper-silver minerals. We took sam- ples from the seven mines we visited in this area, and one from another mine was supplied us. None of the samples contained as much as 0.0001 percent BeQ. They are described below. 328-800 Channel sample across 6-ft vein at portal of lower adit at Gertrude mine, 2 miles south of Ouray (quartz, fluorite, pyrite, galena, and sphalerite). Chip sample across iron-copper deposit at Dunmore mine on Silver Creek 1 mile south of Ouray (cir- cular chimney deposit 200 ft in diameter containing hematite, chalcopyrite, quartz, barite, chlorite, and rhodochrosite). Chip sample across tungsten deposit at Dunmore mine (chimney 20 by 50 ft containing huebnerite, galena, sphalerite, and milky quartz). 5-ft channel sample across vein at North Star mine, 1,000 ft southeast of Dunmore mine (quartz, pyrite, rhodochrosite, rhodonite, galena, and sphalerite). Grab sample from dump of Chrysolite mine, 1,500 ft east of Dunmore mine (galena, sphalerite, quartz, rhodonite, rhodochrosite, and calcite). Grab sample of galena and sphalerite in quartz gangue from dump of Connie mine, 1,600 ft east of North Star mine. . 802 804 806 807 810 176 811 Channel sample across vein at portal of lower adit, Daniel Bonanza mine, on west side of Uncompahgre Canyon, 3,000 ft southwest of Bear Creek falls (galena, sphalerite, pyrite, quartz, rhodonite, and rhodochrosite). 814 2-ft channel sample across vein at Natalie mine, 800 ft northeast of Daniel Bonanza mine (galena and sphalerite in gangue of quartz and rhodochrosite). _______ Lead-zine ore from Mountain Monarch mine, about 1 mile up Uncompahgre River from U. S. Highway 550. Sample furnished by Sherman Comstock of Golden, Colo. PARK COUNTY TARRYALL DISTRICT The Tarryall district is on the east slope of Mount Silverheels about 5 miles west of Como in the north- west part of Park County. The mines are accessible by roads up Tarryall Creek and its tributaries. De- scriptions of the geology and ore deposits are given by Muilenburg (1925), and Singewald (1942). The sedi- mentary rocks are a series of conglomerates, shales, sandstones, and limestones that range in age from Pennsylvanian to Cretaceous. Monzonite porphyry of Tertiary age occurs as sills, dikes, and small stocks in the sedimentary rocks of Paleozoic age, which are met- amorphosed near the intrusive bodies. The ore de- posits are chiefly in the contact zones and consist of veins and replacement bodies that formed at relatively high temperature. The deposits have been mined for their gold content but production has been small. Sev- eral mines were visited in Australia, Montgomery, and French Gulches; the samples obtained are described in table 75. TaBur 75.-Beryllia in samples from the Tarryall district BeO Sample Description (percent) 328-603 K.Grab sample of tactite containing garnet, epidote, and magnetite from dump of Links mine, at head of Australia Gulch 3 miles east of Mount Silverheels_ ___ __ 606 Grab sample of epidote rock containing pyrite, chalcopyrite, and magnetite from dump of Iron mine in small gulch be- tween Little French Gulch and Dead- wood Gulch... {1C 608 - Grab sample of garnet-epidote tactite with a little pyrite from altered limestone bed, north side of Little French Gulch, about - 3 1500 ft west of fron mine...._..._____ 611% Grab sample of garnet-epidote tactite con- taining magnetite and pyrite from dump at abandoned adit half a mile west of junction of north and south forks of Little French _._ 612 - 5-ft channel sample across lime silicate rock containing phlogopite, near contact of quartz monzonite sill exposed at portal of adit (same locality as for 328-61 1..; 614 Grab sample from dump of abandoned mine at east edge of Johnson village, near head of Montgomery Gulch (garnet, epi- dote, diopside, quartz, pyrite, and 0 0. O01 <. 0001 . 0004 <. 0001 . O01 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES PITKIN COUNTY REDSTONE AREA A grab sample of coal from the Mesaverde formation of Late Cretaceous age was collected at a mine 4 miles south of Redstone on State Highway 327. The coal ash contained 0.0005 percent beryllium, 0.004 percent gal- lium, and 0.01 percent vanadium. SAGUACHE COUNTY BONANZA DISTRICT The Bonanza district centers around the mining camp of Bonanza in the northern part of the Cochetopa Hills 15 miles north of Saguache. A basement com- plex of Precambrian granites, schists, and gneisses con- tains infolded and infaulted, limestones, sandstones, and shales that range from Ordovician to Permian in age. Several thousand feet of Tertiary rhyolites, ande- sites, latites, and breccias unconformably overlie the older rocks. Two types of veins are present in the dis- trict: quartz veins containing lead, zinc, silver, and gold, and quartz-rhodochrosite-fluorite veins with minor quantities of sulfides, mined primarily for silver. The geology and ore deposits were described by Patton (1916) and Burbank (1932). A grab sample (828-112) of dump rock was taken at the Eagle mine, 2 miles southeast of Bonanza. The mine is abandoned, and the workings are inaccessible. The most conspicuous gangue minerals on the dump are fluorite, quartz, rhodochrosite, and manganese oxide; the ore minerals are galena, sphalerite, and chalcopy- rite. The sample did not contain as much as 0.001 per- cent BeQO. A chip sample (328-114) was taken across several hundred feet of zunyite-bearing altered volcanic rocks from the north side of Greenback gulch. Analysis of the sample did not show as much as 0.001 percent BeQO. SAN JUAN COUNTY EUREKA-ANIMAS FORKS DISTRICT The Eureka-Animas Forks district as here defined in- cludes Mastadon, California, and Eureka Gulches and the area about the townsites of Eureka and Animas Forks. The geology and mineral deposits have been de- scribed by Ransome (1901b, p. 174-184), and Burbank (in Vanderwilt, 1947, p. 433-485). The rocks exposed in this area are part of the Silverton volcanic series with the exception of a few small intrusive bodies of Tertiary rhyolite and latite. Rhodonite, quartz, and base-metal sulfides occur in veins along strong north- east-trending faults. Helvite was reported from the Sunnyside mine near Eureka by Burbank (19832). Eight mines in the district were examined and sampled. LOCALITIES IN COLORADO Helvite was not noted except at the Sunnyside mine and the quantity there apparently is minute. Descriptions of the samples and analytical results are given in table T6. Tasus 76.-eryllia in samples from the Eureka- Animas Forks district BeO Description (percent) Composite grab sample from dump of Sun- nyside mine (rhodonite, rhodochrosite, galena, sphalerite, and fluorite)......... Channel sample across 5 ft of rhodonite in vein on main adit level at Sunnyside mine 200 ft in from Channel sample across 2 ft of rhodonite in vein on main adit level at Sunnyside mine, 250 ft in from portal____-_-_-_----.- Grab sample of rhodonite and sulfide ore from dump of Sound Democrat mine near head of Mastadon Gulch. 1 mile west of Animas Forks_.______--------- Channel sample across 5-ft rhodonite zone in vein at Silver Queen mine, 500 ft west of Sound Democrat mine..__--------- Chip sample across 6-ft rhodonite zone in vein at Golden Prince mine a few hun- dred feet west of Silver Queen mine__-. Chi? sample across 2-ft rhodonite vein at eptune mine, near abandoned mill at head of Mastadon Gulch-____-_------- Grab sample from dump of Mountain Queen mine, in California Gulch 2 miles west of Animas Forks (chalcopyrite, ga- lena, sphalerite, quartz, fluorite, and Luis,. Grab sample of rhodonite and sulfide ore from dump of Vermillion mine, north side of California Gulch 1 mile west of Animas: Forks. J. .L :. Grab sample of sulfide ore from dump of Columbus mine at west edge of Animas POTKS LZ... 4% - cece ole lall -la a ole o o ate <. 0001 MINERAL POINT AND POUGHKEEPSMULCH DISTRICTS 'The Mineral Point and Poughkeepsie Gulch districts (Ransome, 1901b, p. 185-189 ; Kelley, 1946 ; Hazen, 1949) adjoin one another in the northern part of San Juan County at the headwaters of the Animas and Uncom- pahgre Rivers. The predominant rocks exposed in the area are latite and rhyolitic flows, tuffs, and breccias of the Silverton volcanic series of Tertiary age. In Pough- keepsic Gulch the Silverton series is underlain by the San Juan tuff, also of Tertiary age. Kelley (1946, p. 289) describes the ore deposits as fissure and cavity fill- ings, breccia-chimney and breccia-dike deposits, and re- placement deposits. Most of the productive veins in the area are in the Silverton series. Gold, silver, lead, zinc, and copper are the principal metals produced. Samples from the dumps of 10 mines in the area are described in the following list : Sample 328-142 <0. 001 144 . 0014 145 j . 0002 830 . 0021 831 <. 0001 832 0002 834 . 0015 838 <. 0001 840 <. 0001 841 328-815 Grab sample containing rhodonite, quartz, galena, and sphalerite from dump of Bill Young mine, 200 ft south of Miners Creek at Mineral Point. 817 Grab sample of sulfide ore in quartz gangue, with minor quantity of rhodochrosite from dump of Un- compahgre Chief mine, about 1,000 ft southeast of . Bill Young mine. 177 819 Grab sample of quartz-rhodonite gangue containing galena, sphalerite, and pyrite from dump of Red Cloud mine, half a mile southeast of Bill Young mine. Grab sample from dump of Eurades mine, 5 miles from U. S. Highway 550 on road to Mineral Point (pyrite, galena, sphalerite, and minor tetrabedrite in quartz gangue). Grab sample of quartz and sulfides from dump of Old _ Lout tunnel at end of road up Poughkeepsie Gulch. Grab sample of sulfide ore in rhodonite-rhodochrosite- quartz gangue from dump of Alaska mine, near head of Poughkeepsie Gulch. Grab sample from dump of Picket mine, north of Lake Como at head of Poughkeepsie Gulch (quartz, pyrite, and barite, with minor quantities of galena and sphalerite). Grab sample of quartz and sulfides with some rhodo- nite and rhodochrosite from dump of Amador mine, 3,000 ft northeast of Alaska mine. Grab sample from dump of Poughkeepsie mine, 1.5 miles from end of road up Poughkeepsie Gulch (galena, - sphalerite, tetrahedrite, - chalcopyrite, quartz, rhodonite, and rhodochrosite). Grab sample from dump of Alabama mine, 3,000 ft north of Poughkeepsie mine (galena, sphalerite, pyrite, chalcopyrite, barite, and quartz). 821 822 824 826 827 828 829 Beryllium was detected in only one of the samples (328-815), which contained 0.0016 percent BeQ; the limit of detection was 0.0001 percent BeQ. SILVERTON DISTRICT 'The Silverton district centers around the town of Sil- verton in the central part of San Juan County. The geology and mineral deposits of the district have been described by Burbank (1933b), Cross, Howe, and Ran- some (1905), and Ransome (1901b). The Tertiary Silverton volcanic series, consisting of andesite, latite, and rhyolite flows and breccias, cover much of the area. In the deep valley south of Silverton, Precambrian schist is exposed below the volcanic rocks. Several quartz monzonite bodies intrude the Tertiary volcanic rocks. Samples collected from the contact zones on Sultan Mountain, and from 4 mills and 3 mines in the Silverton district are described in the following list. Beryllium was not detected in spectrographic analyses of the samples, the limit of detection being 0.0001 per- cent BeQ. 328-151 Grab sample of silicified porphyry containing zunyite from dump of Zuni mine, west side of Anvil Moun- tain. Grab sample of garnet-epidote tactite in Hermosa formation, northeast side of Sultan Mountain. Mill heads from Lead Carbonate mill at Gladstone, 7T miles north of Silverton. Mill heads from custom mill at Howardsville, 4ft channel sample across vein in upper adit of Adams mine, 1 mile southwest of Gladstone (hueb- nerite, pyrite, arsenopyrite, calcite, fluorite, and milky quartz). 154 835 844 847 178 851 Mill heads from Shenandoah-Dives mill, 2 miles east of Silverton. 854 Mill heads from Highland Mary mill, 4 miles south of Howardsville. 857 Grab sample from dump of Mighty Monarch mine, south side of Kendall Mountain at Silverton (galena, sphalerite, pyrite, huebnerite, and quartz). SAN MIGUEL COUNTY OPHIR DISTRICT A brief visit was made in August 1949 to the Ophir mining district in southeastern San Miguel County to obtain samples of mill products from the Silver Bell Mines, Inc., mill at Ophir Loop. Ore from the Silver Bell mine was being processed to obtain a bulk sulfide concentrate of galena, pyrite, sphalerite, and chalco- pyrite. A grab sample (328-868) of mill heads did not contain as much as 0.0001 percent BeQO. SUMMIT COUNTY BRECKENRIDGE DISTRICT The Breckenridge district is near the headwaters of the Blue River, about 60 miles west of Denver. Com- prehensive reports on the geology of the district were given by Ransome (1911), Lovering (1984), and Lover- ing and Goddard (1950, p. 102-122). Precambrian gneiss, schist, and granite are exposed in two small areas to the west and north of Breckenridge. Sedimentary rocks including Pennsylvanian to Cretaceous forma- tions cover most of the district. Tertiary monzonite and quartz-monzonite porphyries intrude the sedimen- tary rocks. Veins along small faults have been mined for lead, zinc, silver, and gold. Small contact-meta- morphic deposits have been worked for copper and gold. A tactite zone in the Morrison formation (Jurassic) is exposed for about 1,000 feet on the north side of French Gulch, 1 mile east of Breckenridge. Lenses and bands of magnetite are interlayered with garnet-epidote tactite. The layers range from less than an inch to several feet in thickness. Two samples of tactite (328- 099 and -101) were taken from a cliff exposure at the eastern end of the zone, near a bend in the road about 1,500 feet southwest of the Wellington mill. A third sample (828-109) was taken near the western end of the zone, a few hundred feet west of where it crosses Gibson Gulch. None of the samples contained as much as 0.0001 percent BeQ. MONTEZUMA DISTRICT The Montezuma district is at the headwaters of the Snake River, about 40 miles west of Denver. The geol- ogy and ore deposits were described by Patton (1909), Lovering (1935), and Lovering and Goddard (1950, OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES p. 122-184). Precambrian granites, gneisses, and schists are exposed over most of the Montezuma quad- rangle, but sedimentary rocks of Mesozoic age are ex- posed in the southwestern corner. Tertiary stocks, dikes, and sills intrude the older rocks and occur in a belt that extends from the southwest part to the north- east part of the quadrangle. The chief ore deposits are in mesothermal veins, which have been mined profit- ably for lead, zinc, and silver. Only the lead-zinc- silver veins at the Silver Wing mine and Burke Tun- nel and the contact zones near Tiger were investigated. The Silver Wing mine, owned by T. E. Martin of Montezuma, is on the east side of Glacier Mountain, about 1 mile south of town. The mine workings are driven southwesterly along a quartz vein that dips 50° NW. Galena, sphalerite, pyrite, barite, and mangano- siderite are the principal vein minerals. The country rock is Swandyke hornblende gneiss of Precambrian age. A grab sample (328-728) of vein material did not contain as much as 0.0001 percent BeQ. The Burke Tunnel is 114 miles south of the Silver Wing mine. The tunnel has been driven northwesterly under Glacier Mountain for the purpose of intercept- ing known veins at depth. Several quartz veins con- taining galena, sphalerite, pyrite, and barite have been cut. A sample (328-729) of ore from one of the veins did not show as much as 0.0001 percent BeQO. One mile south of Tiger between Brown and Sum- mit Gulch, the Pierre shale (Cretaceous) has been re- placed by garnet, epidote, actinolite, pyrite, and mag- netite near the contact of a Tertiary quartz monzonite stock, A grab sample (328-721) of the tactite from the dumps of the Cashier mine and a chip-channel sample (828-722) across a 6-foot-wide tactite zone near the portal of the Cashier mine did not contain as much as 0.0001 percent BeQ. UPPER BLUE RIVER DISTRICT The Upper Blue River district, about 5 miles south of Breckenridge, is bounded on the east and south by the Park Range, on the west by the Tenmile Range, and on the north by the Breckenridge mining district. The geology of this district has been described briefly by Singewald (in Vanderwilt, 1947, p. 343-346 and 1951, p. 1-73). The sedimentary rocks include dolomite, shale, quartzite, and limestone of Cambrian to Missis- sippian age, which crop out on the east flank of the Tenmile Range. The core of the range consists of Pre- cambrian granite, gneiss, and schist. Tertiary por- phyries occur as dikes and sills in the older rocks. The ore bodies generally are localized along faults ; they are veins and replacement deposits containing gold, silver, lead, zinc, copper, tungsten, and molybdenum. A con- LOCALITIES IN CENTRAL UNITED STATES tact-metamorphic deposit at the Vanderbilt mine and veins at the Governor mine were sampled. 'The Vanderbilt mine is 10 miles south of Brecken- ridge on State Highway 9. The mine is principally a gold producer, although ore from the dump contains small quantities of galena and sphalerite in a gangue of silicified limestone, diopside, pyrite, specularite, and some quartz. Analysis of a grab sample (328-724) from the dump did not show as much as 0.0001 per- cent BeOQ. The Governor mine is 6 miles south of Breckenridge near State Highway 9. Silver has been produced from a quartz vein in Pennsylvanian and Permian strata. A grab sample (328-727) from a dump, consisting of galena, sphalerite, pyrite, molybdenite, and quartz, did not contain as much as 0.0001 percent BeQ. TELLER COUNTY CRIPPLE CREEK DISTRICT Six samples of mill products were obtained from the Golden Cycle mill at Colorado Springs in 1942 for the Mine, Mill, and Smelter Survey. Virtually all of the ore represented by these samples was from mines in the Cripple Creek district, a detailed description of which was given by Loughlin and Koschmann (1935). The sampling data are shown in table T7. No samples from the Cripple Creek district were analyzed for this investigation. Tasis 77.-Beryllia in samples from the Golden Cycle mill 0 Sample Description (pg-coed) 5-GC-1 Gold concentrates-__________---------- 0. 005 2 Mill heads, gold ore-_________--------- . 005 3 Roaster dust, gold refinery.____-------- Not found 4 Flue dust, gold . O1 5 Refinery byproduct (easily removed gold has been extracted) _______----------- . O01 6 Refinery slag (from roaster).____-------- . 002 CENTRAL UNITED STATES By L. A. Warner and V. R. Wirmrart® Several areas in the central United States were ex- amined during November 1948 (fig. 57). Samples of feldspathoidal igneous rocks were taken at several places in central Arkansas. Spectrographic analyses indicate that beryllium is present in relatively high con- centrations in some of the rocks at Magnet Cove, Ark., but the volume of these rocks is probably not large and the beryllium may not be recoverable. Many of the ore deposits in the Tri-State lead-zine district were sampled, but no beryllium was found in any of them. 179 IL L I NOUS e K A N S A S TRI-STATE DIS TRIGT LITTLE ROCK MAGNET GOll/E 6 e \ l OKLAHOMA} 1 I I LJ I I MISS ISS IP P I N ervrant-BavxiTre 200 Miles ccd Ficurs 57.-Index map showing localities sampled in the Central United States. ARKANSAS MAGNET COVE The igneous complex at Magnet Cove (fig. 58) is a composite intrusive body about 3 miles in diameter. In cross section it is saucer-shaped, with the more resistant rocks forming a rim that surrounds the less resistant central part. The geology has been described by Hal- ton (1929), Landes (1931), Spencer (1946), Washing- ton (1900), and Williams (1891, p. 163-343). Sedimen- tary rocks of Devonian and Mississippian age surround the complex and form irregular inclusions within it. Landes (1931, p. 322) has divided the igneous rocks into three types: (1) the cove intrusives consisting of ijolite and biotite-ijolite, (2) the ridge intrusives con- sisting of foyaite, shonkinite, and leucite porphyry, and (3) the dike rocks which include pegmatites, tin- guaites, monchiquites, and fine-grained - porphyries. Jacupirangite is considered as part of the cove in- trusive. A detailed study was made of the area near Cove Creek bridge (fig. 59). Marble containing coarse cal- cite, monticellite, magnetite, wollastonite, rutile, sphene, idocrase, and pyrite is exposed in a quarry northwest of the bridge. The limestone has been intruded by a 180 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES EXPLANATION Largely covered by alluvium ose Shale and sandstone Metamorphosed rocks mul Tinguaite dikes Monchiquite dikes h1 TN 3 x #. Biotite ijolite Crs Jacupirangite FiGurE 58. -Geologic map of Magnet leucite-syenite dike and a nepheline-eudialyte pegma- tite. The leucite-syenite dike averages 10 feet in width and extends from Cove Creek northwest to the north side of the quarry where it is covered by dump material. The 14-foot-wide nepheline-eudialyte pegamatite is best exposed in the road cut just west of the bridge. Small crystals of eudialyte were noted in the pegmatite. Tufa Hill, a large deposit of siliceous sinter, is about 200 feet north of the road. A small body of ijolite is ex- posed on the east side of the hill. Contacts in this area are covered. Five samples were collected near Cove Creek bridge. Elsewhere in the Magnet Cove area, samples of nearly all igneous rock types were obtained. The samples are described in table 78; sampling localities are shown on figures 58 and 59. The only samples that contain appreciable quantities of beryllium are 329-293, of altered marble from the road cut west of Cove Creek bridge and 328-313, of After H. S. Washington, 1900, plate 24 1 Mile I Locality number see table 78 Cove, Ark., showing localities sampled. TaButs 78.-Beryllia in samples from Magnet Cove, Ark. Locality No. BeO on fig. 58 _ Sample! Rock type (percent) 1 328-305: Leucite porphyry. 0. 0002 2 307 - Leucite tinguaite dike._____________ . 0005 3 309 Nepheline syenite porphyry dike____ . 002 4 315, ShonkMnIbC...2 .. eral reel .. . 002 5 212 Biotite :" . 00083 6 313 Altered biotite ijolite.____________. . 007 T. 815° Lencite porphyry . 0001 8 ol? .c. : . O01 9 S109 : x t'" . 001 10 320: . O01 8285-208 ilicated marble... . 028 204 - Nepheline eudialyte pegmatite... __. . 002 299 - Marmorized limestone.______.____._ . 002 500 . Rilicated . O01 809 ' Sillceous sinter... . 003 1 Localities of samples 328-203 to -303 are shown on figure 59. altered biotite ijolite from the stream bed in front of the Baptist church, east of Cove Creek bridge. The nature of the beryllium-bearing material in the samples has not been determined. Thus far no beryllium min- LOCALITIES IN EASTERN UNITED STATES ® EXPLANATION . 328-303 f Nepheline-eudialyte pegmatite TRUE NORTH MAGNETIC NoRTH r + + + + 4+ i + Leucite syenite Hjolite Limit of outcrop 328-299 f Locality sampled and number Geology by L. A. Warner and V. R. Wilmarth, November 1949 100 0 200 Feet £ 9004s CCO 1 2 59.-Geologic sketch map of area in vicinity of Cove Creek bridge, Magnet Cove, Ark. erals have been reported from Magnet Cove, and it seems probable that the beryllium occurs as an acces- sory constituent in other minerals. LITTLE ROCK AREA An intrusive mass composed chiefly of pulaskite, shonkinite, and foyaite is exposed about 3 miles south of Little Rock on U. S. Highway 167. A grab sample (328-323) of pulaskite from the Big Rock quarry did not contain as much as 0.001 percent BeQO. BRYANT AND BAUXITE AREAS By W. T. HornsER In eastern Saline County, near Bryant and Bauxite, several masses of nepheline syenite intrude folded sedi- mentary rocks of Paleozoic age. The syenite is the source of large bauxite deposits. Tinguaite dikes cut the nepheline syenite in NELA sec. 2, T. 2 S., R. 14 W., southwest of Bryant (Hilde- brand, 1949). The dikes are in four zones that are traceable for 2,000 feet in a northeasterly direction. They contain aegirite, nephelite, sodalite, and alkali feldspars; some show orbicular structures. Three samples (329-842, -843, -844) collected by F. A. Hildebrand of the U. S. Geological Survey were analyzed spectrographically for beryllium. Sample 329-842, from the centers of the orbicles, and sample 329-843, from the matrix of the orbicles, contained 0.002 percent BeOQ. Sample 329-844, a composite of 12 samples of the dike rock, contained 0.000X percent BeO. 181 TRLSTATE LEAD-ZINC DISTRICT In 1942, the U. S. Geological Survey sampled 42 mines and mills in the Tri-State lead-zine district. The analytical results of this sampling appeared to indicate that beryllium is concentrated in the lead-zine ores of this district. The BeQO content of the samples was as high as 0.3 percent by weight. In 1948 Warner and Wilmarth spent 2 weeks in the Tri-State district samp- ling mines and mills, in an effort to determine the mode of the beryllium occurrence and its distribution in the lead-zinc ores. Many of the localities previously sampled were revisited and duplicate materials ob- tained. Spectrographic analyses of 23 representative samples from the district showed no beryllium, the lower limit of detection being 0.001 percent BeQ; and several reanalyses proved the accuracy of these results. The samples that were analyzed are listed below. 828-257 261 Grab sample mill heads, Rialto mill, Treece, Kans. Grab sample of stope fill, Peck and Gregory ming, Commerce, Okla. Dump rock from Bonnet ming, Hockersville, Okla. Dump rock from Roanoke mine, Baxter Springs, Kans. Dump rock from E. L. Bullard mine, Galena, Mo. Ore from Little Ben mine, Waco, Mo. Ore from Richie mine, Waco, Mo. Ore from Crutchfield property, Carl Junction, Mo. Ore from Trilby mine, Granby, Mo. Mill tailings from Federal mill, Granby, Mo. Ore from Dungy mine, Stark City, Mo. Do. Ore from Pioneer mine, Stark City, Mo. Ore from Bluebird mine, Spurgeon, Mo. Ore from Olsen mine, Spring City, Mo. Ore from Mutual mine, Oronogo, Mo. 'Ore from Wingfield mine, Oronogo, Mo. Ore from Federal-Duenweg mill, Duenweg, Mo. Ore and gangue from Katy C mine, Carterville, Mo. Ore from Buckingham mine, Carterville, Mo. Ore from mine 750 ft south of Capital mill, Stotts City, Mo. Ore from Craig-Owens No. 1 mine, Wentworth, Mo. Mill tailings from Sciota mill, Webb City, Mo. 264 267 268 281 283 285 824 825 826 827 828 330 334 339 340 343 345 347 851 354 855 EASTERN UNITED STATES By W. T. Homser Information on nonpegmatite beryllium was ob- tained for six localities in Maine, New Hampshire, New Jersey, and Virginia (fig. 60). These are mainly lo- calities from which beryllium-bearing minerals had been reported previously. Deposits relatively rich in beryllium occur at Iron Mountain, N. H., and along Trish Creek, Va., but the reserves may be small. Further sampling is needed in these areas to appraise the commercial possibilities. - Beryllium occurs in willemite and other minerals at Franklin, N. J. The 182 EXPLANATION & Localities sampled in present investigation nv"\ /. \ X / 1 Other sampling ( o / Localities having samples / containing more than 0.005 1 N E M A beryllia L y . {f 1 0 hys l/ai‘? ave ie. (1, {N H © I N E W YORK/MASS _-_.» CONN ;R! L _’:;\_—MB_1 l - # f if ~As List or LocaLities _ .} i DEL 1 - Sanford, Maine 2 Iron Mountain, N. H. v IRG INI a) 3 - Red Hill, N. H. \ / m6 4 Beemerville, N. J. x led ® 5 - Franklin, N. J. A\/ V I R G I N 1 A ~6 - Irish Creek, Va. areal ali at o F1iGuRE 60.-Index map showing nonpegmatite beryllium occurrences investigated in the Eastern United States. tonnage is large but the grade is low, and much of the beryllium may not be recoverable. SANFORD, YORK COUNTY, MAINE Beryllian idocrase occurs at Sanford, Maine, as dark greenish-brown prismatic crystals as much as 2 cm thick and 6 ecm long, with pinacoidal terminations. The prisms are deeply striated and the crystals have a parting parallel to the faces, seeming to follow growth zones. The crystals grew at random or in radial clusters in openings that were later filled with quartz and calcite. - The idocrase-bearing rock overlies an epi- dote-rich tactite. The geology of the deposit has not been described. According to the geologic map of Katz (1917, pl. 61), the locality is near the contact of the Rindgemere formation of Pennsylvanian(?) age and the Biddeford granite, which is thought to be related to the White Mountain magma series of Billings (1934). The locality was not visited during the present in- vestigation but a specimen from the Cornell University mineralogical collection . (CUM 893-26) was spectro- graphed by A. A. Chodos and found to contain 0.009 percent BeQ. Earlier spectrographic determinations on idocrase from Sanford by George Steiger (1931, written communication) indicated a trace of BeQ in OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES one sample and none in another. Probably the BeOQ content of the idocrase is irregular but the quantity in the Cornell specimen is considerably above the average for analyzed specimens of this mineral. Although it is doubtful that the idocrase is of commercial value, other beryllium-bearing minerals commonly occur with beryl- lian idocrase and further investigation of the deposit may thus be warranted. CARROLL COUNTY, NEW HAMPSHIRE IRON MOUNTAIN Helvite-group minerals were reported by Wadsworth (1880) from an iron ore prospect near Bartlett, N. H. The locality is on the south slope of Iron Mountain at an altitude of about 2,000 feet. A road leading to the mountain turns west from State Highway 16 at Jack- son. The deposit was not visited during the present study, but samples and geological data were furnished by D. M. Henderson of the University of Illinois. The following description was taken largely from his notes. The Iron Mountain deposit is in the Conway granite, of Mississippian(?) age, near its contact with gneisses of the Littleton formation of Early Devonian age. The mine workings consist of a 45-foot adit and a small opencut. The ore body is very irregular but its elonga- tion is approximately parallel to a northwest-trending joint set that may have partly controlled the deposi- tion. In the opencut, the body is about 20 feet wide and 50 feet long. Magnetite and hematite are the chief ore minerals and appear to have formed by replacement of granite. Quartz is abundant in small irregular aggregates and veinlets and in vuggy lenses as much as 3 feet across. Irregular streaks and veinlets containing galena, chal- copyrite, fluorite, and quartz are common in the iron ore. 2 Danalite occurs in irregular aggregates in the ore, much of it as apparent reaction rims around quartz. Well-formed octahedral crystals occur in a few places. Most of the crystals are 2 or 3 mm across and are zoned, consisting of a yellow core and a red-brown rim. Re- fractive indices (Glass, Jahns, and Stevens, 1944, p. 183-185) indicate that the yellow material is probably helvite and the red material danalite. Descriptions and analyses of Henderson's samples are given in table 79. The analyses indicate that the beryllium content of the deposit is probably high and that the granite is relatively rich in niobium. Because of its small size, the deposit is not likely to be of com- mercial interest unless further prospecting in the re- gion adds to the reserves. LOCALITIES IN EASTERN UNITED STATES 79.-Beryllia and niobfigm Pin samples from Iron Mountain, [Quantitative spectrographic analyses by K. J. Murata] Sample ® BeO Nb (percent) (percent) 329-850c Description Composite of 2 samples from inside of adit, and 1 from 30 ft south of the portal, all in fresh biotite graDite_ Composite of 2 samples from the contacts of the zone of iron min- erallzntion......--...._.L.- «l == Composite of chips taken at inter- - vals of 1 to 2 ft across the zone of iron mineralization___._.-------- 0.0017 - 0. 02 852¢ 1/0 . 02 853¢ 1. 6 <. O1 RED HILL Red Hill is an alkalic ring complex 3 miles in diam- eter, just west of State Highway 25 at the north end of Lake Winnipesaukee. As described by Quinn (1937, 1944) the rocks are all syenites, of coarser grain to- ward the outside. Principal minerals are microperthite and hastingsite, with some biotite. An inner ring about half a mile wide contains as much as 30 percent nephe- line and sodalite; some of the rocks in the center of the complex contain quartz. The rocks of Red Hill in- trude the Winnipesaukee quartz diorite of Precam- brian ( ?) to Carboniferous age, but the contacts are no- where exposed. Specimens of the Red Hill rocks were collected in May 1950, in the course of other geologic work. Sam- ple 329-812 from a pit known as the "Horne quarry," in the inner ring contained only 0.000X percent Be (spectrographic analysis by A. A. Chodos). The rock is coarse-grained syenite composed of abundant early nepheline, albitized microperthite, and hastingsite, with streaks and veinlets of later sodalite (Quinn, 1937, p. 384-387). Wohlerite (NaCa, (Zr,Nb) FSi,0;) is sparingly present (Pirsson and Washington, 1907, p. 270-271). Sample 829-818 was of coarser grained hornblende syenite without nepheline and is probably equivalent to Quinn's "outer coarse syenite" (Quinn, 1937, p. 383-385; chemical analysis on p. 380). Spec- trographic analysis did not detect any beryllium in the sample, the limit of sensitivity being 0.000X Be. SUSSEX COUNTY, NEW JERSEY BEEMERVILLE AREA Feldspathoidal rocks are common around the village of Beemerville, south of State Highway 23 and west of Sussex, N. J. The geology of the area was described by Aurousseau and Washington (1922), Milton **, Wil- kerson (1946), and Davidson." Recently the commer- @ Milton, Charles, 1929, Nepheline syenite and related rocks of the Franklin Furnace quadrangle, New Jersey : Johns Hopkins Univ. Ph. D. thesis. "% Davidson, E. S., 1948, The Geological relationships and petrography of a nepheline syenite near Beemerville, Sussex County, N. J.: Rutgers Univ. M. Sc. thesis. 183 cial uses of these rocks were appraised by Parker (1948, p. 52-57) and Wilkerson and Comeforo (1946). The main intrusive body extends 2 miles along the eastern face of Kittatinny Mountain, where it apparently was intruded as a thick sill-like mass between the Martins- burg shale of Ordovician age and the Shawangunk con- glomerate of Silurian age. Most of this body is a granular syenite composed of nepheline, orthoclase, and aegerite-augite, with minor amounts of biotite, sphene, magnetite, sodalite, garnet, apatite, and fluorite. At least 25 sills and dikes intrude the Martinsburg shale and the Precambrian formations within a few miles of Beemerville. They have been classified as nepheline syenite (tinguaite and bostonite), lamprophyre (min- ette or camptonite), and diabase. Samples were obtained from the main mass and sev- eral of the smaller bodies on June 13, 1950. Through the courtesy of J. H. C. Martens of the New Jersey Bureau of Mineral Research, samples from the bureau's collections also were made available for analysis. The analyzed samples are described in table 80. TABLE 80. -Beryllium in samples from the Beemerville urea, New Jersey [Spectrographic analyses by A. A. Chodos except No. -828] B Sample Location ! Description (partied) 329-826 2084.8 N., 845.7 E.; Specimen{[of boston- 0. Oo X Parker 102; ite dike orfsill. Wilkerson 12. 827 2083.2 N., 841.5 E.; Specimen of porphy- - . OOX Parker 103; ritic nepheline Wilkerson 15. syenite from dike. 828 2090.3 N., 844.5 E.; Sample of nepheline 3. 002 Parker 99; syenite from main Davidson 38. mass. $29 2090.6 N., 844.9 E.; - Sample of biotite- . O00 X Parker 99; rich nepheline Davidson 46. syenite from main mass. 830 2089 N., 849.7 E.; Composite of three . O0OX Parker 100; specimens of Wilkerson 1; nepheline syenite Milton and from sill.* Davidson. 1 Location according to U. S. 1,000-yd grid system, as shown on Branchville quadrangle, numbered b 1:81,680, U. y Parker (1948 1948, The geological relationship Beemerville, Sussex County, N. J.: Rutgers Univ. M. Davidson (1950). 2 Mode is given 37, aegirite-augite 11, biotite 2, sphene 3, magnetite and pyrite 3. $ Analyzed by J. K. Murata for BeQO, in percent. 4 Average of 3 modes by Wilkerson, in S. Army Corps of Engineers, 1943. Localities also as , pl.1); Wilkerson (1952, fig. 1); Davidson (Davidson, E. 6. s and petrography of a nepheline syenite near . Sc. thesis); and Milton and by Davidson (idem.), in percent: nepheline 43, potassium-feldspar percent (personal communication from J. H. C. Martens, 1950): nepheline 45, potassium-feldspar 34, aegirite-augite 18, sphene 2, and magnetite 1. FRANKLIN DISTRICT The Franklin district, one of the largest producers of zinc ore in the United States, is between Franklin and Ogdensburg on the western edge of the Precambrian New Jersey Highlands. In June 1950, the district was visited and samples were obtained through the courtesy of the New Jersey Zinc Co. and with the cooperation of D. W. Jenkins and L. H. Bauer of the chemical de- 3 ‘ I | | 184 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES partment, and A. W. Pinger and E. N. Newcomb of the geological department. Analytical geological data on the occurrence of beryllium in the district were also made available by the company. The geology, mineralogy, and ore deposits of the Franklin district have been described in roughly 300 reports; among the more recent are those by Kerr (1933), Palache (1935), and Pinger (1948). The dis- trict is almost entirely within the Franklin limestone of Precambrian age, which was metamorphosed to a white, coarse, calcitic marble and squeezed into sharp northward-plunging folds. At the north end of the district the Precambrian formations are unconform- ably overlain by limestone and quartzite of Paleozoic age. The two producing mines of the district are the Franklin mine at Franklin and the Sterling Hill mine at Ogdensburg. At both mines zinc ore occurs in tab- ular masses that are conformable to synclines in the Franklin limestone. The composition of the ore is ap- proximately 40 percent franklinite, 25 percent gangue carbonates, 23 percent willemite, 11 percent gangue sili- cates, and 1 percent zincite. The distribution of the ore minerals is remarkably uniform throughout the ore bodies; the distribution of gangue silicates is less uni- form. Pyroxene is fairly common at both mines; gar- net and rhodonite are common at Franklin and rare at Sterling where tephroite is more widespread. Granite pegmatite occurs at Franklin but has not been identified at Sterling Hill. Some of the pegmatite apparently is earlier than the ore and some later. The pegmatite is pink to gray and composed of quartz, or- thoclase, microcline, albite, and micoperthite, with some hornblende, pyroxene, epidote and sphene. Complex tactite deposits containing rhodonite, hardystonite, manganoan-zincian pyroxenes, garnet, mica, and rare silicates appear to be localized at places where ore is associated with pegmatite. Palache and Bauer (1930) described barylite and beryllian idocrase from Franklin, and chemists of the New Jersey Zinc Co. have found traces of beryllium in other minerals. In the present investigation, an attempt was made to determine the distribution of beryllium in the ore. Analytical data for the mill products are shown in table 81. A magnet and heavy liquids were used to prepare mineral separates from the ore and mill prod- ucts, The BeQ contents of these samples, together with results of other workers, are given in table 82. The analyses indicate that the ore from Franklin is higher in beryllium content than that of Sterling Hill. Most of the beryllium is in the willemite concentrate and probably is contained in willemite. The average grade of the concentrate appears to be much too low for it to TaBur 81.-Beryllia in mill products from the Franklin district @ \ Franklin mine Sterling Hill mine BeO BeO Material Sample (percent) Sample (percent) Crude ore: ._ 329—832 0.003 329-837 0. 001 Franklinit - rato clude. af.. B8B <. 0004 83s _. oo1 ______ (. 005) 839 002 Willemite-franklin- ite product_.____ { 836 (- 8858 yrs t uo iy Willemit n iim aera ta yn. frste t"" "Sof 03 #40 . 0005 ______ (. 025-0 8:3)6 ( 8875) Haans iiss k fier ue . 000 84 04 Tailings..___.____- 1 B52 ( dole yy at's (.: 0006) 1 Numbered analyses made by A. A. Chodos of composite samples for the period 1940-44, submitted by the New Jersey Zinc Co. Unnumbered analyses (in paren- theses) made by New Jersey Zinc Co. in 1944 (Laboratory Report 160) of composites of similar products from a single month in 1941, have been as a probable source of beryllium. The other beryllium-bearing minerals at Franklin are present only in small quantities. Barylite, a rare beryllium barium silicate, that con- tains as much as 15.77 percent BeQ is known only on the 400-foot level of the Franklin mine (Palache and Bauer, 1930, p. 32). Small white plates of barylite em- bedded in hedyphane (a calcium-lead-chloro-arsenate) occur in a layered vein. The succession of layers from vein wall inward are : brown calcite and native copper; gray calcite; a thin zone of willemite and serpentine; white calcite; and barylite, hedyphane, and willemite. There are two types of beryllium-bearing idocrase at the Franklin mine. That containing the most beryllium "occurs in the form of slender brown prisms embedded in a coarsely crystalline mixture of green willemite, brown garnet, leucophoenicite, and barite with subordi- nate amounts of svabite, native copper, and gageite" (Palache and Bauer, 1930, p. 30). Analyses by F. A. Gonyer of two specimens of brown idocrase from the mine showed 1.56 and 3.95 percent BeQ (Table 85). A blue to blue-green idocrase, known as "cyprine," con- tains from 1 to 2 percent copper and as much as 0.11 percent BeQ. As described by Palache (1935, p. 95), it occurs for the most part as fibrous crystals associated with garnet, calcite, willemite, biotite, bustamite, and native copper in granular tactite. A large pocket of this variety of idocrase was found in 1920 on the 850- foot level of the Franklin mine, but on the whole it is rare. Both idocrase and calcite replace coarse calcite (Ries and Bowen, 1922, p. 561). In discussing the ido- crase at the Franklin mine, Palache (1935, p. 95) states, "It now appears certain that the beryllium is not geneti- cally associated with the primary willemite ore, but is a postore element introduced into the deposit from in- trusive pegmatites." While it is probably true that the beryllium-bearing idocrase is a postore mineral, whose LOCALITIES IN EASTERN UNITED STATES 185 Tasos 82.-Beryllia in minerals from the Franklin district Species Location ! Sample ® BeO (percent) Analyst and reference Franklinite.....- F 329-833A <0. 0004 . A. A. Chodos________._--- SH 838A <<0004, Willemite._......- F 834A . 004 .._. .2. OL rads SH 840A 005 +:}... 0.2 sr F 834B «£.0004: ..... 10. . EMIR tees Rhodonite....-... F CUM-335-2 002 .._... AOL 2 = nem PX) . 0O0X Goldschmidt and Peters, 1932, p. 868. Tephroite....... F CUM-379-1 <.0004 A. A,. Chodos.___________. Garnet.......... F 329-815A <. 0004 -.. «~ (10. ee a nas Pyroxene........ ¥ 8198 OL "* a 10... .ir I2... cta ne= Pol cg. <. 001 - Goldschmidt and Peters, 1932, p. 368. Sphalerite.._..... SH CUM-58-42 <. 0004 A. A. Svabite......... F 329-817A <, 0004 ..... 818A 2001 E ecco ms 819A <.0004 ...=. 402. .- ans aan Apatite.:_...... CUM-549-114 <.0004 ___.. do:. Hill. At ne csa Idocrase.._...... F. i% 1. 56 F. A. Gonyer (C. S. Hurl- but, Jr.,. written com- munication, 1951). _____________ 3. 95 Ges 00... .e _____________ . 04 A. A, _____________ S11 Sandell, 19408, p. 675---.-- Barylite......... P. c es 15. 77 Bauer (Palache and Bauer, 1930, p. 32). Remarks No visible impurities. Do. One percent garnet and dark inclusions. One percent impurities, including cloudy altered products. One percent impurities, inclusions. One percent impurities. including dark No impurities except cloudy altered products. Two percent anisotropic inclusions. One percent inclusions and alteration products. No visible impurities. One percent inclusions and alteration prod- ucts; trace of garnet. Three percent inclusions and alteration products. One percent inclusions and alteration products. Three percent inclusions and alteration products. Brown variety. Do. Blue griety (cyprine); 1 percent garnet. o. 1 F, Franklin mine; SH, Sterling Hill mine. j 2 Separates from samples of corresponding number in table 81. presence depends on the proximity of pegmatite and ore, the source of the beryllium is not known. No beryl has been noted in the pegmatites at Franklin. A specimen of pyroxene from the 1,050-foot level of the Franklin mine was found to contain 0.01 percent BeQ. The pyroxene, tentatively identified as zincian- manganoan diopside, occurs in a coarse-grained aggre- gate of willemite, svabite, and leucophoenicite. Minor quantities of beryllium are contained in rhodonite and svabite. IRISH CREEK DISTRICT, ROCKBRIDGE coUNTY, VA. The tin-beryllium-bearing quartz veins of the Irish Creek district, Virginia, were described by Koschmann, Glass, and Vhay (1942). The locality was not visited during the present investigation. The country rock of the district is Precambrian and consists of gneiss and granodiorite with small dikes of aplite and basic rock. The known quartz veins are restricted to the granodio- rite and are as much as 9 feet wide, though commonly less than a foot wide. Bordering the veins on one or both sides are greisen layers as much as 5 feet thick. Four periods of mineral deposition with intervening 467945-59--13 periods of fracturing are recognized. Quartz was de- posited during the first stage; cassiterite, muscovite, beryl, and wolframite during the second stage; musco- vite, siderite, ankerite, fluorite, biotite, phenakite, and chlorite during the third stage; and nontronite, vermic- ulite, hematite, montmorillonite, clinozosite, and cal- cite during the fourth stage (Koschmann, Glass, and Vhay, 1942, p. 271). Pale-green to yellow beryl crystals as much as 2 ecm long are most abundant at the edges of the quartz veins, although minor quantities of small beryl crystals are disseminated in the greisen. According to Glass (oral communication, 1950), the green beryl forms a border along the quartz-greisen contact and is a replacement of quartz. A chemical analysis of the green beryl by R. E. Stevens showed 12.33 percent BeO. Phenacite occurs as irregular grains and as pseudomorphs after beryl; it is generally associated with chlorite (Kosch- mann, Glass, and Vhay, 1942, p. 282). The reserves of beryl in the Irish Creek district were not determined. However, the beryl is sufficiently coarse grained to make it recoverable if the vein ma- terial is milled for tin. : 186 SELECTED REFERENCES Adams, J. E., Newell, N. D. Wills, N. H., and others, 1949, The Permian rocks of the Trans-Pecos region: West Texas Geol. Soc. Guidebook 4. Adams, J. W., 1953, Beryllium deposits of the Mount Antero re- gion, Chaffee County, Colorado: U. S. Geol. Survey Bull. 982-D, p. 95-119. Ahrens, L. H., and Liebenberg, W. R., 1950, Tin and indium in mica, as determined spectrochemically : Am. Mineralogist, v. 85, p. 571-578. Aldridge, W. N., and Liddell, H. F., 1948, Microdetermination, of beryllium with particular reference to its determination in biological materials: Analyst, v. 73, p. 607-613. Allen, E. T. and Clement, J. K., 1908, The role of water in tremolite and certain other minerals: Am. Jour. Sci., 4th ser., v. 26, p. 101-118. Anderson, C. A., 1948, Structural control of copper mineraliza- tion, Bagdad, Arizona : Am. Inst. Mining Metall. Engineers Trans., v. 178, p. 170-180. porphyry copper deposit, Arizona: Econ. Geology, v. 45, p. 609-628. 1950b, Lead-zine deposits, Bagdad area, Yavapai County, Arizona, in Arizona zine and lead deposits: Arizona Bur. Mines Bull. 156, p. 122-138. Arppe, A. E., 1861, Analyser af finska mineralier : Acta Aoc. Sci. Fennicae, v. 6. Aurand, H. A., 1920, Fluorspar deposits of Colorado: Colorado Geol. Survey Bull. 18. Aurousseau, M., and Washington, H. S., 1922, The nephelite syenite and nephelite porphyry of Beemerville, N. J.; Jour. Geology, v. 30, p. 571-586. Baker, C. L., 1927, Exploratory geology of a part of southwest- ern Trans-Pecos Texas: Texas Univ. Bull. 2745. Barrell, Joseph, 1907, Geology of the Marysville mining district, Montana: U. S. Geol. Survey Prof. Paper 57. Barth, T. F. W., 1926, Die Kristallographische Bezichungawis- chen Helvin and Sodalit.: Norsk geol. tidsskr., Band 9, p. 40-42. Bateman, P. C., 1945, Pine Creek and Adamson tungsten mines, Inyo County,‘ Calif.: California Jour. Mines and Geology, v. 41, p. 281-249. Bateman, P. C., Erickson, M. P., and Proctor, P. D., 1950, Geol- ogy and tungsten deposits of the Tungsten Hills, Inyo County, Calif.: California Jour. Mines and Geology, v. 46, no. 1, p. 23-42. Bechamp, A., 1866, Analyse de Veau mineralle sulfureuse des Fumades (source Therese) : Acad. sci. [Paris] Comptes ren- dus, v. 62, p. 1088-1090. Beck, Richard, 1904, Uber die Erzlager der Umbegung von Schwarzenberg im Erzgeberg, II : Jahrb. berg. huttenwesen k. Sachsen, 1904A, p. 56-96. Becker, R. B., and Gaddum, L. W., 1937, The composition of limonites effective and ineffective in correcting bush sick- ness in cattle: Jour. Dairy Sci., v. 20, p. 7837-739; Chem. Abs., 1938, v. 82, col. 1304. Beckwith, R. H., 1989, Asbestos and chromite deposits of Wy- oming: Wyoming Geol. Survey Bull. 29. Beede, J. W., 1918, Notes on the geology and oil possibilities of the northern Diablo Plateau in Texas: Texas Univ. Bull. 1852 [1920]. 1950a, Alteration and metallization in the Bagdad‘ OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Beeler, H. C., 1911, Asbestos deposits of Casper Mountain, Wyo.: Colorado School Mines Mag., v. 1, no. 10, p. 5-9, and no. 11, p. 5-9. Behre, C. H., Osborn, E. F., and Rainwater, E. H., 1936, Contact ore deposition at the Calumet iron mine of Colorado : Econ. Geology, v. 31, p. 781-804. Bergeat, Alfred, 1909, Der Granodiorit yon Concepcion del Oro im Staate Zacatecas [Mexico] und seine Contact-bildugen : Neues Jahrb., Beilage-Band 28, p. 421-573. Billings, M. D., 1984, Paleozoic age of the rocks of central New Hampshire : Science, new ser., v. 79, no. 2038. Binyon, E. O., Holmes, G. H., Jr., and Johnson, A. C., 1950, In- vestigation of the Tem Piute tungsten deposit, Lincoln County, Nevada; U. S. Bur. Mines Rept. Inv. 4626. Borovick, S. A., and Gotman, J. D., 1939, Content of rare and other elements in the cassiterites of different genesis from U. S. S. R. deposits according to spectrum analysis data ; Acad. sci. U. R. S. S., Comptes rendus, (Doklady) v. 23, no. 4, p. 851-854. Bowen, N. L., 1940, Progressive metamorphism of siliceous lime- stone and dolomite: Jour Geology, v. 48, p. 225-274. Bragg, W. L., and Brown, G. B. 1926, Die Kristalistruktur von Chrysoberyll (BeAl:O,) : Zeitschr. Kristallographie, Band 63, p. 122-143. Bragg, W. L., and West, J., 1926, The structure of beryl, BesAl: SiO): Royal Soc. [London] Proc., v. 111A, p. 691-714. Bragg, W. L., and Zachariasen, W. H., 1930, The crystalline structure of phenakite and willemite: Zeitschr. Kristal lographie, Band 72, p. 518-528. Brannock, W. W., Fix, P. F., Gianella, V. P., and White, D. E., 1948, Preliminary geochemical results at Steamboat Springs, Nevada: Am. Geophys. Union Trans., v. 29, p. 211- 226. Bray, J. M., 1942a, Distribution of minor chemical elements in Tertiary dike rocks of the Front Range, Colo.: Am. Mineral- ogist, v. 27, p. 425-440. 1942b, Spectrographic distribution of minor elements in igneous rocks from Jamestown, Colo.: Geol. Soc. America Bull., v. 53, p. 765-814. , Brown, W. H., 1926, The mineral zones of the White Cross dis- trict and neighboring deposits in Hinsdale County, Colo.: Colorado School Mines Mag., v. 15, no. 11, p. 5-15. Buerger, M. J., 1948, The role of temperature in mineralogy ; Am. Mineralogist, v. 33, p. 101-121. Burbank, W. S., 1980, Revision of geologic structure and strati- graphy in the Ouray district Colorado, and its bearing on ore deposition: Colorado Sci. Soc. Proc., v. 12, p. 151-232. 1932, Geology and ore deposits of the Bonanza mining district, Colorado: U. S. Geol. Survey Prof. Paper 169. 1933a, The manganese minerals of the Sunnyside veing, Eureka Gulch, Colo.: Am. Mineralogist, v. 18, p. 518-527. 1933b, Vein systems of the Arrastre Basin and regional geologic structure in the Silverton and Telluride quad- rangles, Colorado: Colorado Sci. Soc. Proc., v. 13, p. 135- 214. 1940, Structural Control of ore deposition in the Un- compahgre district, Ouray County, Colo., with suggestions for prospecting : U. S. Geol. Survey Bull. 906-E, p. 189-265. Butler, B. S., and Loughlin, G. F., 1916, A reconnaissance of the Cottonwood-American Fork mining region, Utah: U. S. Geol. Survey Bull. 620-1, p. 165-226. SELECTED REFERENCES Butler, B. S., Loughlin, G. F., Heikes, V. C., and others, 1920, The ore deposits of Utah: U. S. Geol. Survey Prof. Paper 111. Butler, B. S., and Vanderwilt, J. W., 1933, The Climax molyb- denum deposit, with a section on history, production, met- allurgy, and development, by C. W. Henderson: U.. 8. Geol. Survey Bull. 846-C, p. 195-237. Butler, B. S., Wilson, E. D., and Rasor, C. A., 1938, Geology and ore deposits of the Tombstone district, Arizona : Arizona Bur. Mines Bull. 143. Caglioti, V., and Zambonini, F., 1928, Ricerche chimiche sulla rosterite di San Piero in Campo (Isola d'Elba) e sui berilli in general: Gazz, chim, Italiana, v. 58, p. 131-152; Chem. Abs., 1928, v. 22, col. 2580. Calkins, F. C., and Emmons, W. H., 1915, Description of the Philipsburg quadrangle, Montana : U. S. Geol. Survey Geol. Atlas, Folio 196. Cameron, E. N., Jahns, R. H., McNair, A. H., and Page, L. R. 1949, Internal structure of granitic pegmatitites: Econ. Geology Mon. 2. Carne, J. E. 1911, Tungsten-mining industry in New South Wales: New South Wales Geol. Survey, Mineral Resources Ser., no. 15, p. 58, 67. Carobbi, Guido, and Pieruccini, Renzo, 1941, Sopra i constituenti minori di alcune rocee sedimentarie di Passo delle Radioci (Appennino Tosco-Emiliano) : Spectrochimica Acta, Band 2, p. 32-44; Chem. Abs., 1942, v. 36, col. 5737. Chhibber, H. L., 1945, An unusual occurrence of beryl near Narhual, Patiala State: Jour. Sci. Indus. Research [New Delhi], v. 3, p. 423. Clabaugh, S. E., 1950, Eudialyte and eucolite from southern New Mexico [abs.]: Am. Mineralogist, v. 35, p. 279-280. Clark, J. W., 1950, Minor metals: beryllium, in Minerals Year- book, 1948: U. S. Bur. Mines, p. 1311-1318. Clarke, F. W., 1910, Analyses of rocks and minerals : U. S. Geol. Survey Bull. 419. Clayton, J. E., 1888, The Drumlummon group of veins and their mode of formation: Eng. Mining Jour., v. 46, p. 85-86, 106-108. Collins, G. E., 1931, Localization of ore bodies at Rico and Red Mountain, Colorado, as conditioned by geologic structure and history: Colorado Sci. Soc. Proc., v. 12, p. 407-424. Collins, R. F., 1949, Volcanic rocks of northeastern New Mex- ico: Geol. Soc. America Bull., v. 60, p. 1017-1040. Comeforo, J. E., Hatch, R. A., and Eitel, Wilhelm, 1950, Iso- morphism of synthetic fluorine-amphiboles [abs.]: Geol. Soc. America Bull., v. 61, p. 1452. Connolly, J. P., 1927, Tertiary mineralization of the Northern Black Hills: South Dakota Bur. Mines Bull. 15. Cooper, J. R., 1950, Johnson Camp area, Cochise County, Ari- zona, in Arizona zinc and lead deposits: Arizona Bur. Mines Bull. 156, p. 30-39. Cornu, Eugene, 1919, Etude spectrographique des cendres de plantes marines: Acad. sci. [Paris] Compte rendus, v. 168, p. 513-514. Correns, C. W., and Engelhardt, W. V., 1938, Neue Untersuchun- gen liber die Verwittering des Kalifeldspates: Naturwiss., Band 26, p. 137-138. Coulton, C. C., 1936, The platinum group discovery at Centen- nial, Wyo.: Mining Jour., v. 20, no. 6, p. 5. Crane, G. W., 1915, Geology of the ore deposits of the Tintic mining district, Utah: Am. Inst,. Mining Metall. Engineers Bull. 106, p. 2147-2160. 187 1923, Geological and mineralogical conditions prevailing in the Tintic district, Utah: Salt Lake Mining Rev., v. 25, no. 10, p. 12-14. Crawford, R. D., 1913, Geology and ore deposits of the Monarch and Tomichi districts, Colorado: Colorado Geol. Survey Bull. 4, p. 317. Crawford, R. D., and Worcester, P. G., 1916, Geology and ore deposits of the Gold Brick district, Colorado: Colorado Geol. Survey Bull. 10, 116 p. Creasey, S. C., and Quick, G. L., 1943, Copper deposits of a part of the Helvetia mining district, Pima County, Arizona: TU. S. Geol. Survey open-file report, 34 p. Cross, Whitman, 1897, Igneous rocks of the Leucite Hills and Pilot Butte, Wyo.: Am. Jour. Sci., 4th ser., v. 4, p. 115-141. Cross, Whitman, Howe, Ernest, and Irving, J. D., 1907, De- scription of the Ouray quadrangle, Colorado: U. S. Geol. Survey Geol. Atlas, Folio 153. Cross, Whitman, Howe, Ernest, and Ransome, F. L., 1905, De- scription of the Silverton quadrangle, Colorado : U. S. Geol. Survey Geol. Atlas, Folio 120. Cross, Whitman, and Ransome, F. L., 1905, Description of the Rico quadrangle, Colorado: U. S. Geol, Survey Geol. Atlas, Folio 130. Cross, Whitman, and Shannon, E. V., 1927, The geology, petrog- raphy, and mineralogy of the vicinity of Italian Mountain, Gunnison County, Colo.: U. S. Nat. Mus. Proc., v. T1, art. 18. Cross, Whitman, and Spencer, A. C., 1900, Geology of the Rico Mountains, Colorado: U. S. Geol, Survey 21st Ann. Rept., 1899-1900, pt. 2, p. 7-165. Cucci, M. W., Neuman, W. F., and Mulryan, B. J., 1949, Quan- titative study of reaction between beryllium and quinizarin- 2-sulfonic acid: Anal. Chemistry, v. 21, p. 1358-1360. Dana, J. D., 1892, A system of mineralogy, 6th edition: New York, John Wiley and Sons, 1134 p. Darton, N. H., 1916, Geology and underground water of Luna County, New Mexico: U. S. Geol. Survey Bull. 618. 1925, A résumé of Arizona geology: Arizona Bur. Mines Bull. 119. 1928, "Red beds" and associated formations in New Mexico; with an outline of the geology of the State: U. S. Geol. Survey Bull. 794. i Darton, N. H., and Siebenthal, C. E., 1909, Geology and mineral resources of the Laramie Basin, Wyoming: U. S. Geol Survey Bull. 364. Diemer, R. A., 1941, Titaniferous magnetite deposits of the Laramie Range, Wyo.: Wyoming Geol, Survey Bull, 31. Diller, J. S., 1911a, Types, modes of occurrence, and important deposits of asbestos in the United States: U. S. Geol Survey Bull. 470-K, p. 505-524. 1911b, Occurrence of asbestos in Wyoming: Mineralog. Sci., v. 63, p. 447-448. Dunham, K. C., 1935, The geology of the Organ Mountains, with an account of the geology and mineral resources of Dona Ana County, N. Mex.: New Mexico School Mines Bull. 11. Eakle, A. S., 1917, Minerals associated with the erystalline limestone at Crestmore, Riverside County, Calif.: Cali- fornia Univ. Publ., Geology Dept. Bull., v. 10, p. 327-360. Eardley, A. J., and Hatch, R. A., 1940, Proterozoic rocks in Utah: Geol. Soc. America Bull., v. 51, p. 795-844. Eckel, E. B., Williams, J. S., and Galbraith, F. W., 1949, Geology and ore deposits of the LaPlata district, Colorado: U. 8. Geol. Survey Prof. Paper 219. 188 Eitel, Wilhelm, Hatch, R. A., and Humphrey, R. A., 1950, Iso- morphism of synthetic fluorine-micas: Am. Cryst. Assoc. Abs. of First Mtg., State College, Pa., p. 17. Emmons, S. F., 1903, Platinum in the copper ores in Wyoming: U. S. Geol. Survey Bull. 218, p. 94-97. Emmons, S. F., Cross, Whitman, and Eldridge, G. H., 1894, Description of Anthracite-Crested Butte quadrangle, Colo- rado : U. S. Geol. Survey Geol. Atlas, Folio 9. Emmons, W. H., 1908, Geology of the Haystack stock, Cowles, Park County, Montana: Jour. Geology, v. 16, p. 193-229. Emmons, W. H., and Calkins, F. C., 1913, Geology and ore de- posits of the Philipsburg quadrangle, Montana : U. S. Geol. Survey Prof. Paper 78. Emmons, W. H., and Larsen, E. S., Jr., 1913, The hot springs and mineral deposits of Wagon Wheel Gap, Colo.: Econ. Geology, v. 8, p. 235-246. i 1923, Geology and ore deposits of the Creede district, Colorado: U. S. Geol. Survey Bull. 718. Fairbairn, H. W., 1948, Packing in ionic minerals: Geol. Soc. America Bull., v. 54, p. 1305-1374. Farmin, Rollin, 1933, "Pebble dikes" and associated mineraliza- tion at Tintic, Utah: Econ. Geology, v. 28, no. 6, p. 601-606. Feigl, Fritz, 1989, Qualitative analysis by spot tests, inorganic and organic applications, 24 ed.: New York, Nordemann Publishing Co. Fersman, A. E., 1929, Geochemische Migration der element: Abh. prakt. Geol. and Bergwirtschaftslehre, Band 18. 1940, Pegmatiti: Akad. Nauk SSSR Izv., Moskva-Len- ingrad. Filippov, A. N., and Tolmacey, Yu. M., 1935, On the presence of rare alkaline metals in amazonites: Akad. Nauk SSSR Compte rendu (Doklady), new ser., v. 1, p. 323. Fischer, H., 1928, Der Nachweis and die Bestimmung geringer mengen, Beryllium mit Hilfe Chinalizarin: Zeitschr. anal. Chemie, Band 73, p. 54-64. Fischer, Walther, 1925, El yacimiento de Helvine de Casa la Plata: Acad. nac. cienc. Cordoba Boll., v. 28, p. 133-178. --- 1926, Die Helvin Lagerstitte yon Casa la Plata (Sierra de Cordoba, Argentinien). Centralbl. Min., 1926A, p. 32-42. f 1942, Helvin und Phenakit aus dem Stockgranit von Hil- bersdorf, Kreis Gorlitz: Naturf. Gesell, Gorlitz, Abh., Band 33, Hefte 3, p. 5-11. f Fleischer, Michael, and Cameron, E. N., 1946, U. S. Geol. Survey, Trace Elements Inv. Rept. 29, issued by the U. S. Atomic Energy Comm., Tech. Inf. Service, Oak Ridge, Tenn., 27 p. Fletcher, M. H., and White, C. E., 1946, A simple test for the detection of the beryllium minerals: Am. Mineralogist, v. 31, p. 82-83. Fletcher, M. H., White, C. E., and Sheftel, M. S., 1946, Deter- mination of beryllium in ores: Indus. and Eng. Chemistry, Anal. ed., v. 18, p. 183. Folinsbee, R. E., 1941, Optical properties of cordierite in rela- tion to alkalies in the cordierite-beryl structures: Am. Min- eralogist, v. 26. p. 485-500. Fowler, K. S., 1930, The anorthosite area of the Laramie Moun- tains, Wyo.: Am. Jour. Sci., 5th ser., v. 19, p. 305-315, 373- 403. Freeman, G. O., 1942, Spectrographic data concerning the pres- ence of less common elements in rocks : Am. Mineralogist, v. 27, p. T76-779. Freise, F. W., 1931, Untersuchung von Mineralen auf Abnutz- barkeit bei Verfrachtung in Wasser : Mineralog. und petrog. Mitt., Band 41, p. 1-7. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Fresenius, L., 1933, Uber die Bestimmung der in sehr geringen Mengen vorhanden Bestandteile der naturlichen Mineral- wasser: Deutsche geol. Gesell. Zeitschr., Band 85, p. 540- 544. f Fries, Carl, Jr., 1940, Tin deposits of the Black Range, Catron and Sierra Counties, New Mexico: U. S. Geol. Survey Bull. 922-M, p. 855-370. Fries, Carl, Jr., and Butler, A. P., Jr., 1943, Geologic map of the Black Range tin district, New Mexico: U. S. Geol. Survey Strategic Minerals Inv. Maps. Furnival, G. M., 1939, Notes on quartz "dikes": Am. Mineral- ogist, v. 24, p. 499-507. Giadeke, Rudolf, 1938, Die gesetzmassigen Zusammenhange und Anomalien in der Vesuviangruppe und einigen anderen Kalksilikaten: Chemie der Erde, Band 11, 592-636. Gale, H. S., 1910, Coal fields of northwestern Colorado and northeastern Utah: U. S. Geol. Survey Bull. 415. R Gardner, J. H., 1909, The coal field between Durango, Colorado, and Monero, New Mexico: U. S. Geol. Survey Bull. 341-C, p. 852-363. Gaudin, A. M., Dasher, John, Pannell, J. H., and Freyberger, W. L., 1950, Use of an induced nuclear reaction for the concentration of beryl: Am. Inst. Mining Metall. Engineers Trans., v. 187, p. 495-498. f Geller, R. F., Yavorsky, P. J., Steierman, B. L., and Creamer, A. S., 1946, Studies of binary and ternary combinations of magnesia, calcia, baria, beryllia, alumina, thoria, and zir- conia in relation to their use as porcelains: U. S. Nat. Bur. Standards Jour. Research, v. 36, p. 277-812. Genth, F. A., 1892, Contributions to mineralogy, No. 54, with Crystallographic notes by S. L. Penfield: (6) Danalite: Am. Jour. Sci., v. 44, p. 385 Gerasimovsky, V. I., 1939, Lovozerite, a new mineral: Akad. Nauk SSSR Doklady, v. 25, p. 753-756; Mineralog. Abs., v. 7, p. 468, 1940. Gibson, F. H., and Selvig, W. A., 1944, Rare and uncommon elements in coal: U. S. Bur. Mines Tech. Paper 669. Gillerman, Elliot, 1952, Fluorspar deposits of Burro Mountains and vicinity, New Mexico: U. S. Geol. Survey Bull. 973-F, p. 261-289. Gilluly, James, 1982, Geology and ore deposits of the Stockton and Fairfield quadrangles, Utah: U. S. Geol. Survey Prof. Paper 173. 1941, Thrust faulting in the Dragoon Mountains, Ariz. [abs.] : Geol. Soc. America Bull., v. 52, p. 1949. Glass, J. J., 1985, The pegmatite minerals from near Amelia, Va.: Am. Mineralogist, v. 20, p. 741-768. Glass, J. J., Jahns, R. H., and Stevens, R. E., 1944, Helvite and danalite from New Mexico, and the helvite group: Am. Mineralogist, v. 29, p. 163-191. Glass, J. J., and Smalley, R. G., 1945, Bastnaesite: Am, Min- eralogist, v. 30, p. 601-615. Goddard, E. N., 1936, The geology and ore deposits of the Tin- cup mining district, Gunnison County, Colorado: Colorado Sei. Soc. Proc., v. 18, no. 10, p. 551-595. Goddard, E. N., chn., 1948, Rock color chart: Natl. Research Council, Washington, D. C. Goldich, S. S., and Berquist, H. R., 1947, Aluminous lateritic soil of the Sierra de Bahoruco area, Dominican Republic, West Indies: U. S. Geol. Survey Bull. 953-C, p. 53-84. Goldschmidt, V. M., 1911, Kontaktmetamorphose in Kristiani- agebiet: Norske vidensk.-akad. Oslo Skr. I Mat.-natury. Kl., no,.1. SELECTED REFERENCES 1934, Drei Vortriige fiber Geochemie : Geol. foren, Stock- holm Forh., Band 56, p. 385-427. 1937, Principles of distribution of chemical elements in minerals and rocks: Jour. Chem, Soc. London, p. 655-678. Goldschmidt, V. M., Hauptmann, H., and Peters, CL, 1933, Uber die Berucksichtigung "seltener'" Elemente bei Gesteinsana- lysen: Die Naturw., Jahr, p. 362-365. Goldschmidt, V. M., and Peters, CL, 1932, Geochemie des Beryl- liums: Gesell. Wiss. Gottingen, Math.-phys. KI, Nachr., Heft 4, p. 360-376. 1933, Uber die Anreicherung seltener Elemente in Stein- kohlen: Gesell. Wiss. Gottingen, Math.-phys. Kl, Nachr,, Heft 4, p. 371-387. Goodale, C. W., 1915, The Drumlummon mine, Marysville, Mon- tana: Am. Inst. Mining Metall. Engineers Trans., v. 49, p. 258-283. Graf, D. L., and Kerr, P. F., 1950, Trace-element studies, Santa a Rita, N. Mex.: Geol. Soc. America Bull., v. 61, p. 1023-1052. Griggs, R. L., 1948, Geology and ground-water resources of the eastern part of Colfax County, N. Mex.: New Mexico Bur. Mines Ground-Water Rept. 1. Grigoriey, D. P., and Iskull, E. W., 1937, The regeneration of amphiboles from their melts at normal pressure: Am. Min- eralogist, v. 22, p. 169-177. Gruner, J. W., 1944, Simple tests for the detection of the beryl- lium mineral helvite: Econ. Geology, v. 39, p. 444-4417. Gustavson, S. A., and Umhau, J. B., 1951, Tin, in Minerals Yearbook, 1949: U. S. Bur. Mines, p. 1193-1219. Haberlandt, Herbert, 1944, Concentration of rare elements in mineral formations due to additions of organic origin: Forsch. u. Fortschr., Band 20, p. 154-155; Chem, Abs., 1949, v. 43, col. 2187. Halton, W. L., 1929, Magnet Cove, Arkansas and vicinity: Am. Mineralogist, v. 14, p. 484-487. Hanley, J. B., Heinrich, E. W., Page, L. R., and others, 1950, Pegmatite investigations in Colorado, Wyoming, and Utah : TU. S. Geol. Survey Prof. Paper 227. . Harder, E. C., 1909, The Taylor Peak and Whitepine iron-ore deposits, Colorado: U. S. Geol. Survey Bull, 380-E, p. 188-198. Harley, G. T., 1984, The geology and ore deposits of Sierra County, N. Mex.: New Mexico Bur. Mines Bull. 10. Harley, G. T., 1940, The geology and ore deposits of north east- ern New Mexico: New Mexico Bur. Mines Bull. 15. Hartley, W. N., 1902, Notes on quantitative spectra of beryl- | lium: Royal Soc. London Proc., v. 69, p. 283-285. Hawley, J. B., Lewis, C. L., and Wark, W. J., 1951, Spectro- graphic study of platinum and palladium in common sul- fides and arsenides of the Sudbury district, Ontario: Econ. Geology, v. 46, p. 149-162. Hazen, S. W., 1949, Lead-zine-silver in the Poughkeepsie district and part of the Upper Uncompahgre and Mineral Point districts, Ouray and San Juan Counties, Colorado: U. S. Bur. Mines Rept. Inv. 4508. Hermann, R., 1848, Untersuchungen russischen Mineralien. 32. Uber das Vorkommen und die Zusammensetzung der sibiri- schen Vesuviane: Jour. prakt. Chemie, Band 44, p. 193-208. Hernon, R. M., 1949, Geology and ore deposits of Silver City region, N. Mex.: West Texas Geol, Soc. Guidebook, Field Trip no. 3. Hess, F. L., 1908, Tungsten, nickel, cobalt, etc., in Mineral Re- sources of the United States, 1908, part I : U. S. Geol. Sur- vey, p. 721-749. 189 1926, Platinum near Centennial, Wyo.: U. S. Geol. Sur- vey Bull. 780-C, p. 127-135. Hess, F. L., and Larsen, E. S., 1921, Contact-metamorphic tung- sten deposits of the United States: U. S. Geol. Survey Bull. T25-D, p. 245-309. Hewett, D. F., 1937, Helvite from the Butte district, Montana : Am. Mineralogist, v. 22, p. 803-804. Hewett, D. F., Callaghan, Eugene, Moore, B. N., and others, 1986, Mineral resources of the region around Boulder Dam: U. S8. Geol. Survey Bull. 871, 197 p. Hildebrand, F. A., 1949, Orbicular tinguaite dikes from near Bryant, Saline County, Arkansas [abs.] : Geol. Soc. America Bull., v. 60, p. 1896. Hill, J. M., 1909, Notes on the economic geology of southeastern Gunnison County, Colorado: U. S. Geol. Survey Bull. 380-A, p. 21-40. Hill, R. S., 1946, Exploration of Grey Eagle, Grandview, and Royal John Claims, Grant and Sierra Counties, N. Mex.: U. S. Bur. Mines Rept. Inv. 3904. Hillebrand, W. F., 1905, Red beryl from Utah: Am. Jour. Sci., 4th ser., v. 169, p. 330-8331. Hillebrand, W. F., and Lundell, G. E. F., 1929, Applied inorganic analysis: New York, John Wiley and Sons. ms Hills, R. C., 1899, Description of Elmoro quadrangle, Colorado : U. S. Geol. Survey Geol. Atlas, Folio 58. ; 1900, Description of Walsenburg quadrangle, Colorado : U. S. Geol. Survey Geol. Atlas, Folio 68. j Hobbs, S. W., 1944, Tungsten deposits in the Boriana district and the Aquarius Range, Mohave County, Arizona: U. S. Geol. Survey Bull. 940-1, p. 247-264. ' Hoffman, G. C., 1901, Danalite : Canada Geol. Survey Ann. Rept., vy, 12R, p. 15. Holland, H. D., and Kulp, J. L., 1949, The distribution of acces- sory elements in pegmatites ; I Theory: Am. Mineralogist, v. 84, p. 35-60. Holser, W. T., 1950, Metamorphism and related mineralization in the Philipsburg region, Montana: Geol. Soc. America Bull., v. 61, p. 1053-1090. 1953, Beryllium minerals in the Victorio Mountains, Luna County, N. Mex.: Am. Mineralogist, v. 38, p. 599-611. Howell, J. V., 1919, Twin Lakes district of Colorado [Lake and Pitkin Counties] : Colorado Geol. Survey Bull. 17. Huffington, R. M., 1948, Geology of the northern Quitman Moun- tains, Trans-Pecos Texas: Geol. Soc. America Bull., v. 54, p. 987-1047. Hulin, C. D., 1925, Geology and ore deposits of the Randsburg quadrangle, California : California Div. Mines Bull. 95. Hunt, S. F., 1928, Cambrian rocks, structures and ore deposits in Tintic mining district, Utah: Salt Lake City Mining Rev., v. 29, no. 21, p. 13-15. Huntington, J. H., 1880, Iron ore at Bartlett, N. H.: Boston Soc. Nat. History Proc., v. 20, p. 288-292. Hutton, C. A., 1950, Studies of detrital minerals: Geol. Soc. America Bull., v. 61, p. 635-716. Irving, J. D., 1905, Ore deposits of the Ouray district, Colorado : U. S. Geol. Survey Bull. 260, p. 50-77. Irving, J. D., and Bancroft, Howland, 1911, Geology and ore deposits near Lake City, Colorado: U. S. Geol. Survey Bull. 478. Iwase, Eiichi, and Ukai, Nabuo, 1944, Alteration of beryl: Tokyo Inst. Phys. Chem. Research Bull., v. 23, p. 393-399. Jaffe, H. W., 1951, The role of yttrium and other minor elements in the garnet group: Am, Mineralogist, v. 36, p. 183-155. 190 Jahns, R. H., 19442, Beryllium and tungsten deposits of the Iron Mountain district, Sierra and Socorro Counties, New Mexico: U. S. Geol. Survey Bull. 945-C, p. 45-79. 1944b, Ribbon rock, an unusual beryllium-bearing tactite : Econ. Geology, v. 89, p. 173-205. 1948, Masses of pegmatite quartz [abs.] : Geol. Soc. America Bull., v. 59, p. 1374. Jannasch, P., 1884, Zur Kenntniss der Zusammensetzung des Vesuvians: Neues Jahrb, Min. Pet. Geol., 1884, Band 1, p. 269-270. Jenney, C. P., 1935, Geology of the central Humboldt Range, Nevada: Nevada Univ. Bull., v. 29, no. 6. Johnson, V. H., 1949 Geology 'of the Helvetia mining district, Pima County, Arizona [abs.]: Geol. Soc. America Bull., v. 60, p. 1900-1901. Just, Evan, 1926, Emeralds of Bom Jesus dos Meiras: Econ. Geology, v. 21, p. 801-810. Kaiser, B. P., Herring B. F., and Rabbitt, J. C., 1954, Minor elements in some rocks, ores, and mill and smelter products : U. S. Geol. Survey Trace Elements Inv. Rept. 415, U. S. Atomic Energy Comm. Tech. Inf. Service, Oak Ridge, Tenn. Katchenkov, S. M., 1948, Elementary composition of petroleum ashes: Akad. Nauk SSSR Doklady, v. 63, p. 361-363; Chem. Abs., v. 43, p. 2139, 1949. Katz, F. J., 1917, Stratigraphy in southwestern Maine and south- eastern New Hampshire: U. 8. Geol. Survey Prof. Paper 108, p. 165-177. Kawecki, H. C., 1946, The production of beryllium compounds, metal, and alloys : Electrochem. Soc. Trans., v. 89, p. 229-236, 258-259. Kelley, V. C., 1946, Geology, ore deposits, and mines of the Min- eral Point, Poughkeepsie and Upper Uncompahgre districts, Ouray, San Juan, Hinsdale Counties, Colorado: Colorado Sci. Soc. Proc., v. 14, no. 7, p. 289-466. 1949, Geology and economics of New Mexico iron-ore de- posits: New Mexico Univ. Publ. in Geology no. 2, 246 p. Kelley, V. C., Rothrock, H. E., and Smalley, R. G., 1947, Geology and ore deposits of the Gallinas district, Lincoln County, New Mexico: U. S. Geol. Survey Strategic Mineral Inv. Prelim. Map 3-211. Kemp, J. F., and Knight, W. C., 1903, Leucite Hills of Wyoming : Geol. Soc. America Bull., v. 14, p. 305-336. Kennedy, J. S., and O'Meara, R. G., 1948, Flotation of beryllium ores: U. S. Bur. Mines Rept. Inv. 4166. Kerr, P. F., 1933, Zinc deposits near Franklin, New Jersey : In- ternat. Geol, Cong., 16th, United States, Guidebook 8, p. 2-14. 1938, Tungsten mineralization at Oreana, Nevada :; Econ. Geology, v. 83, p. 890-425. 1940, Tungsten-bearing manganese deposit near Gol- conda, Nevada: Geol. Soc. America Bull., v. 51, p. 1359-1389. 1946a, Tungsten mineralization in the United States : Geol. Soc. America Mem. 15. 1946b, Kaolinite after beryl from Alto do Giz, Brazil: Am. Mineralogist, v. 81, p. 485-441. Kerr, P. F., and Callaghan, Eugene, 1935, Scheelite-leuchten- bergite vein in Paradise Range, Nevada: Geol. Soc. Amer- ica Bull. v. 46, p. 1957-1974. Kerr, P. F., Kulp, J. L., Patterson, C. M., and Wright, R. J., mineralization at Oreana, Nevada: Econ. Geology, v. 80, p. ___ 287-800. - Kerr, P. F., Kulp, J. L., Patterson, C. M., and Wright, R. J., 1950, Hydrothermal alteration at Santa Rita, New Mexico : Geol. Soc, America Bull., v. 61, p. 275-347. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Kildale, M. B., 1944, The Tintic district, Utah: Utah Mining Soc. News Bull., v. 5, no. 2, p. 11-19. King, P. B., 1948, Geology of the southern Guadalupe Moun- tains, Texas: U. S. Geol. Survey Prof. Paper 215. 1949, Regional geologic map of parts of Culberson and Hudspeth Counties, Texas: U. S. Geol. Survey Oil and Gas Inv, Prelim. Map 90, scale 1: 150,000. King, P. B., Branson, C. G., and others, 1949, Pre-Permian rocks of Trans-Pecos area and southern New Mexico : West Texas Geol. Soc. Guidebook 5. King, P. B., King, R. E., and Knight, J. B., 1945, Geology of Hueco Mountains, El Paso and Hudspeth Counties, Texas : U. S. Geol. Survey Oil and Gas Inv. Prelim. Map 36. King, P. B., and Knight, J. B., 1944, Sierra Diablo region, Huds- peth and Culberson Counties, Texas: U. S. Geol. Survey Oil and Gas Inv. Prelim. Map 2. Klepper, M. R., 1943, Tungsten deposits of Cherry Creek dis- trict, Nevada: U. S. Geol. Survey Strategic Mineral Inv. Prelim. Maps. Knight, W. C., 1902, Further notes on the occurrence of rare metals in the Rambler mine, Wyoming: Eng. Mining Jour., v. 73, p. 696. Knopf, Adolph, 1913, Ore deposits of the Helena mining region, Montana : U. S. Geol. Survey Bull. 527. 1916, The composition of the average igneous rock : Jour. Geology, v. 24, p. 620-622. 1917, Tungsten deposits of northwestern Inyo County, California: U. S. Geol. Survey Bull. 640-L, p. 220-255. 1924, Geology and ore deposits of the Rochester district, Nevada: U. S. Geol. Survey Bull. 762. 1936, Igneous geology of the Spanish Peaks region, Colorado: Geol. Soc. America Bull., v. 47, p. 1727-1784. 1950, The Marysville granodiorite stock, Montana: Am. Mineralogist, v. 35, p. 834-844. Koenigsberger, J., 1913, Versuch einer Einteilung der ost- alpinen Mineralagerstatten : Zeitschr. Kristallographie, Band 52, p. 166-167. Kolthoff, I. M., 1928, The detection of traces of beryllium and the colorimetric determination of this element: Am. Chem. Soc. Jour., v. 50, p. 393. Koritnig, S., 1951, Ein Beitrag zur Geochemie des Fluor: Geochim. et Cosmochim. Acta, v. 1, p. 89-116. Korzhinsky, D. S., 1937, Dependence of mineral stability on depth: Vses. Mineral. Obshch. Zapiski, v. 46, p. 369-396. Koschmann, A. H., Glass, J. J., and Vhay, J. S., 1942, Tin de- posits of Irish Creek, Virginia: U. S. Geol. Survey Bull. 936-K, p. 271-206. Kossel, G. E., and Neuman, W. F., 1950, Color reaction between beryllium and aurin-tricarboxylic acid: Anal. Chemistry, v. 22, p. 936-939. Kroll, W. S., 1945, Extractive metallurgy of beryllium: U. S. Bur. Mines Inf. Cire. 7826, 15 p. Krumbein, W. C., and Pettijohn, F. J., 1938, Manual of sedimen- tary petrography: New York, D. Appleton Co. Kulesar, F., 1948, How prospectors can detect beryllium in ores : Eng. Mining Jour., v. 144, p. 103. Kuroda, Kazuo, 1939, Occurrence of beryllium in the hot springs of Matunoyama: Japan Chem. Soc. Bull., v. 14, p. 305-306. 1940,Occurrence of beryllium in the hot springs of Japan;: Japan Chem. Soc. Bull., v. 15, p. 237-238. Lagrange, M. R., and Tchakirian, M. A., 1939, Sur le determina- tion spectrographique de quelques elements existant dans certaines algues calcaires: Acad. sci. [Paris] Comptes rendus, v. 209, p. 58-59. SELECTED REFERENCES Lamb, F. D., 1947, Beneficiation of New England beryllium ores : U. S. Bur. Mines Rept. Inv. 4040, 9 p. Landergren, Sture, 1943, Geokemiska studier over Grangesberg- faltets jarnmalmer : Ingenidrsvetenskapsakad. Handl. no. 172. 1948a, On the geochemistry of Mediterranean sediments- Preliminary report on the distribution of beryllium, boron, and the ferrides in three cores from the Tyrrhenian Sea : K. Vetensk. Vitt.-Samh. Handl., 6 Foljden, Ser. B., Band 5, no. 18. 1948b, On the geochemistry of Swedish iron ores and as- sociated rocks: Sveriges geol. undersokning, ser. C, no. 496. Landes, K. K., 1931, A paragenetic classification of the Magnet Cove minerals: Am. Mineralogist, v. 16, p. 313-326. Landon, R. E., 1931, Metamorphism and ore deposition in the Santa Rita-Hanover-Fierro area, New Mexico; a study of igneous metamorphism : Univ. Chicago Abs. of Theses, Sci. Ser., v. 7, p. 229-234. Larionov, J. and Tolmacey, J. M., 1937, On the chemical compo- sition of cassiterites: Acad. Sci. U. R. S. S. Comptes rendus (Doklady) v. 14, p. 303-306. Larsen, B. 8. [Jr.], 1942, Alkalie rocks of Iron Hill, Gunnison County, Colorado: U. S. Geol. Survey Prof. Paper 197-A, p. 1-64. Larsen, B. S. [Jr.], and Berman, Harry, 1934, The microscopic determination of the non-opaque minerals, 24 ed.: U. S. Geol. Survey Bull. 848. Larsen, E. S. [Jr.], and Ross, C. S., 1920, The R and S molyb- denum mine, Taos County, N. Mex.: Econ. Geology, v. 15, p. 567-578. Lasky, S. G., 1936, Geology and ore deposits of the Bayard area, Central mining district, New Mexico: U. S. Geol. Survey Bull. 870. 1938, Geology and ore deposits of the Lordsburg mining district, Hidalgo County, New Mexico: U. S. Geol. Survey Bull. 885. --- 1947, Geology and ore deposits of the Little Hatchet Mountains, Hidalgo and Grant Counties, New Mexico: U. S. Geol. Survey Prof. Paper 208. Lasky, S. G., and Hoagland, A. D., 1948, Central mining district, N. Mex.: Internat. Geol Cong., 18th, London, Repts., pt. 7, p. 97-110. Lasky, S. G., and Wooton, T. P., 1933, The metal resources of New Mexico and their economic features : New Mexico Bur. Mines Bull. 7. f Lausen, Carl, 1981, Geology and ore deposits of the Oatman and Katherine districts, Arizona: Arizona Bur. Mines Bull. 131. Lee, W. T., 1912, Coal fields of Grand Mesa and West Elk Moun- taing, Colorado: U. S. Geol. Survey Bull. 510. 1922, Description of the Raton-Brilliant-Koehler quad- rangle, New Mexico and Colorado: U. S. Geol. Survey Geol. Atlas, Folio 214. Le Grange, J. M., 1980, The Barbara beryls: a study of an oc- currence of emeralds in the northeastern Transvaal, with some observations on metallogenic zoning in the Murchison Range: South Africa Geol. Soc. Trans., v. 82, p. 1-25. Lemmon, D. M., 1941a, Tungsten deposits in the Tungsten Hills, Inyo County, California : U. S. Geol. Survey Bull. 922-Q, p. 497-514. 1941b, Tungsten deposits in the Sierra Nevada near Bishop, California, a preliminary report: U, S, Geol, Survey Bull. 931-6, p. 79-104, 191 Lemmon, D. M., and Dorr, J. V. N., 24, 1940, Tungsten deposits of the Atolia district, San Bernardino and Kern Counties, California: U. S. Geol. Survey Bull. 922-H, p. 205-245. Lewis, H. C., 1882, An American locality for helvite : Acad. Nat. Sci. Philadelphia Proc., p. 101-102. Lindgren, Waldemar, 1908, Notes on copper deposits in Chaffee, Fremont, and Jefferson Counties, Colorado: U. S. Geol. Bull. 340-B, p. 157-174. 1915, Processes of mineralization and enrichment in the Tintic mining district, Utah: Econ. Geology, v. 10, p. 225-240. 1933, Differentiation and ore deposition, Cordilleran region of the United States, in Ore deposits of the Western States (Lindgren volume), p. 152-180: Am. Inst. Mining Metall. Engineers. Lindgren, Waldemar, Graton, L. C., and Gordon, C. H., 1910, The ore deposits of New Mexico: U. S. Geol. Survey Prof. Paper 68. & Lindgren, Waldemar, and Loughlin, G. F., 1919, Geology and ore deposits of the Tintic mining district, Utah: U. S. Geol. Survey Prof. Paper 107. Lopez de Azcona, J. M., and Puig, A. C., 1947, Concentration of 12 trace elements in the ashes of Asturian coals: Inst. geol. minero espafia, Bol., v. 60, p. 3-9; Chem. Abs. v. 42, p. 3551, 1948. Loughlin, G. F., 1917, Zinc carbonate and related copper car- bonate ores at Ophir, Utah : U. S. Geol. Survey Bull. 690-A, p. 1-14. Loughlin, G. F., and Koschmann, A. H., 1935, Geology and ore deposits of the Cripple Creek district, Colorado: Colo. Sci. Soc. Proc., v. 13, no. 6, p. 212-485. Lovering, T. S., 1934, Geology and ore deposits of the Brecken- ridge mining district, Colorado : U. S. Geol. Survey Prof. Paper 176. 1935, Geology and ore deposits of the Montezuma quad- rangle, Colorado: U. S. Geol. Survey Prof. Paper 178. 1949, Rock alteration as a guide to ore-East Tintic district, Utah : Econ. Geology Mon. 1, 65 p. Lovering, T. S., and Goddard, E. N., 1950, Geology and ore deposits of the Front Range, Colorado: U. S. Geol. Survey Prof. Paper 228. Machatschki, Felix, 1930, Die summen formel des Vesuvians und seine Beziehungen zum Granat : Centralbl. Mineralogie, 1930, Abt. A, p. 284-293. 1932, Zur Formel des Vesuvian: Zeitschr. Kristallo- graphie, Band 81, p. 148-152. Mamurovsky, A. A., 1916, Vesuvianite from Bersovsky mines: Moscow Univ., Min. Geol. Cabinet, Sbornik, 1916, p. 88-89; Mineralog. Abs., v. 2, p. 179, 1924. Marks, G. W., and Jones, B. M., 1948, Method for the spec- trochemical determination of beryllium, cadmium, zinc, and indium in ore samples: U. S. Bur. Mines Rept. Inv. 4363, p. 1-11. Martin, G. C., 1910, Coal of the Denver basin, Colorado: U. S. Geol. Survey Bull. 381-C, p. 297-306. Mazade, M., 1851, Mémoire chimique, geognosique, et topo- graphique sur les sources minerales de Nérac; découverte de Pacide mellitique, du tantale, du molybdéne, du tungs- téne et de Vetain, du cerium, de I'yttria et de la glucine dans les eaux minerals: Acad. Sci. [Paris] Comptes rendus, v. 82, p. 685. McConnell, Duncan, 1942, Griphite, a hydrophosphate garnetoid : Am, Mineralogist, v. 27, p. 452-461, f 192 McConnell, Duncan, 1950, The crystal chemistry of montmoril- lonite: Am. Mineralogist, v. 85, p. 166-172. McKnight, E. T., 1982, Rico district, in Colorado : Internat. Geol. Cong., 16th, United States, Guidebook 19, p. 63-65. Meen, V. B., 1939, Vesuvianite from Great Slave Lake Region, Canada: Toronto Univ. Studies, Geol. Ser., no. 42, p. 69-74. Miers, H. A., and Prior, G. T., 1892, Danalite from Cornwall : Mineralog. Mag., v. 10, p. 10-14. Milton, Charles, and Davidson, Norman, 1950, An occurrence of natrolite, andradite, and allanite in the Franklin Furnace quadrangle, N. J.: Am. Mineralogist, v. 85, p. 500-507. Minguzzi, C., 1943, Geochimica applicata : sopra i constituenti minori dei "fanghi rossi" provenenti dalla lavorazione delle | bauxiti istriani: Soc. Mineralog. Italiana, Rendiconti, Anno 2, p. 30-82. Miropolsky, L. M., and Borovick, S. A., 1944, The results of spec- trum analysis of silicon minerals from the Permian deposits of Tartaria: Akad. Nauk SSSR Doklady, new ser., v. 45, p. 334-837. Moraes, L. J., 1933, Beryllium minerals in Brazil: Econ. Geology, v. 28, p. 289-202. Morey, G. W., 1949, Transport and deposition of the non-sulphide vein minerals-III. Phase relations at the pegmatitic stage (discussion) : Heon. Geology, v. 44, p. 151-154. Morgan, R. A., and Hummel, F. A., 1949, Reactions of BeQO and Si0@ syntheses and decomposition of phenacite: Am. Ceramic Soc. Jour., v. 82, p. 250-255. Muilenburg, G. A., 1925, Geology of the Tarryall district, Park County, Colo.: Colorado Geol. Survey Bull. 31. Murdoch, Joseph, and Webb, R. W., 1948, Minerals of California : California Div. Mines Bull. 136. Myers, A. T., and Barnett, P. R., 1953, Contamination of rock samples during grinding as determined spectrographically . Am. Jour. Sci., v. 251, no. 11, p. 814-880. Nazarenko, V. A., 1937, The occurrence of vanadium, beryllium, and boron in the ash of some coals : Akad. Nauk SSSR, Lab. Biogeochem., Trav., v. 4, p. 265, 270 ; Chem. Abs., v. 32, 7700, 1938. Needleman, Stanley, 1954, Beryllium, in Minerals Yearbook 1951 : U. S. Bur. Mines, p. 209-218. Nelson, L. A., 1940, Paleozoic stratigraphy of Franklin Moun- tains, west Texas: Am. Assoc. Petroleum Geologists Bull., v. 24, no. 1. Neumann, Henrich, 1948, On hydrothermal differentiation : Econ. Geology, v. 43, p. 77-83. Newcomb, R. C., 1941, Gray quartz breccia ore body of the High- land mine, Butte, Montana: Econ. Geology, v. 36, p. 185-198. Nockholds, S. R. and Mitchell, R. L., 1948, Geochemistry of some Caledonian plutonic rocks-A study of the relationship be- tween major and trace elements of igneous rocks and their minerals: Royal Soc. Edinburgh Trans., v. 41, p. 533-575. Noddack, Ida, and Noddack, Walter, 1934, Die geochemischen Verteilungskoeffizienten der Element: Svensk Kem. tids- skr., Band 46, p. 173. Norman, G. W. H., 1945, Molybdenite deposits and pegmatites in the Preissac-La Corne area, Abitibi County, Quebec: Econ. Geology, v. 40, p. 1-17. Norton, F. H., 1939, Hydrothermal formation of clay minerals in the laboratory : Am. Mineralogist, v. 24, p. 1-17. Oftedal, Ivar, 1939, Beryllium in radioactive minerals: Norsk geol. tiddsskr., Band 19, p. 341-342. Ogilvie, I. H., 1908, Some igneous rocks from the Ortiz Moun- tains, New Mexico: Jour. Geology, v. 16, p. 230-238. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Olson, J. C., 1942, Mica-bearing pegmatites of New Hampshire: U. S. Geol. Survey Bull. 981-P, p. 363-408. Oppenheim, Victor, 1948, The Muzo emerald zone, Colombia, S. A.: Econ. Geology, v. 43, p. 81-38. Osborn. H. F., 1950, Segregation of elements during the crystal- lization of a magma: Am. Ceramic Soc. Jour., v. 33, p. 219-224. Osborne, G. D., 1932, The metamorphosed limestones and asso- ciated contaminated rocks of the Carlingford district, County Louth: Geol. Mag., v. 69, p. 209-233. Osterwald, F. W., and Osterwald, D. B., 1952, Wyoming mineral resources: Wyoming Geol. Survey Bull. 45. Pabst, Adolf, 1936, Vesuviantite from Georgetown, Calif.: Am. Mineralogist, v. 21, p. 1-10. Page, L. R., and others, 1953, Pegmatite investigations in the Black Hills, South Dakota, 1942-45: U. S. Geol. Survey Prof. Paper 247. Paige, Sidney, 1910, The ore deposits near Pinos Altos, New Mexico: U. S. Geol. Survey Geol. Atlas, Folio 199. 1916, Description of the Silver City quadrangle, New Mexico: U. S. Geol. Survey Geol. Atlas, Folio 199. Palache, Charles, 1907, Mineralogical notes: Am. Jour. Sci., 4th ser., v. 24, p. 249-258. 1929a, Paragenetic classification of the minerals of Franklin, N. J.: Am. Mineralogist, v. 14, p. 1-18. 1929b, A comparison of the ore deposits of Langban, Sweden, with those of Franklin, N. J.: Am. Mineralogist, v. 14, p. 48-47. 1934, Minerals from Topaz Mountain, Utah: Am. Min- eralogist, v. 19, p. 14-16. 1935, The minerals of Franklin and Sterling Hill, Sussex County, New Jersey: U. S. Geol. Survey Prof. Paper 180. Palache, Charles, and Bauer, L. H., 1980, On the occurrence of beryllium in the zinc deposits of Franklin, N. J.; Am. Mineralogist, v. 15, p. 30-33. Palache, Charles, Berman, Harry, and Frondel, Clifford, 1944 (v. 1), 1951 (v. 2), Dana's system of mineralogy, 7th ed.: New York, John Wiley & Sons. Pardee, J. T., 1917, Ore deposits of the northwestern part of the Garnet Range, Montana : U. S. Geol. Survey Bull. 660-F, p. 159-239. Pardee, J. T., and Schrader, F. C., 1983, Metalliferous deposits of the greater Helena mining region, Montana : U. S. Geol. Survey Bull. 842. Park, C. F. Jr., 1985, Copper in the Tintic district, Utah, in Copper resources of the world : Internat. Geol. Cong., 16th, United States, p. 361-367. Park, C. F., Jr., and McKinlay, P. F., 1948a, Geology and ore deposits of Red River and Twining districts, Taos County, N. Mex., a preliminary report: New Mexico Bur. Mines Circ. 18. 1948b, Feldspar introduction in the Red River district, New Mexico [abs.]: Am. Mineralogist, v. 83, p. 204. Parker, J. M., 1948, New Jersey's potential feldspar resources : Rutgers Univ. Bur. Mineral Resources Bull. 5, pt. 1. Parsons, A. B., 1925, The Tintic Standard mine (Tintic district), Utah: Eng. and Mining Jour.-Press, v. 120, no. 17, p. 645- 652. Parsons, C. L., 1909, The chemistry and literature of beryllium : Easton, Pa., Chemical Rubber Publishing Co. Patton, H. B., 1908, Topaz-bearing rhyolite of the Thomas Range, Utah: Geol. Soc. America Bull., v. 19, p. 177-192. SELECTED REFERENCES --- 1909, The Montezuma mining district of Summit County, Colorado: Colo. Geol. Survey, First Ann. Rept., p. 105-145. 1916, Geology and ore deposits of the Bonanza district, Saguache County, Colorado: Colorado Geol. Survey Bull. 9. 1917, Geology and ore deposits of the Platoro-Summit- ville mining district, Colorado: Colorado Geol. Survey Bull. 13. Patton, H. B., Smith, C. E., Butler, G. M., and Hoskin, A. J., 1910, Geology of the Grayback mining district, Costilla County, Colorado: Colorado Geol. Survey Bull. 2. Peer, K. C., 1948, Spectrographic determination of beryllium : Light Metal Age, v. 1, no. 4, p. 14-15, 22. § Pieruccini, Renzo, 1943, Determinazione spettrografica del beril- lio in alcune rocce sedimentaire del' appenino tosco-emil- liano: Spectrochimica Acta, Band 2, p. 269-290 ; Chem. Abs., v. 39, col. 471, 1945. 1950, La mica di un blocco rigettato dal Somma ed i minerali che lVaccompagnano: Soc. Mineralog. Italiana, Rend, an. 6, p. 84. Pinger, A. W., 1948, Geology of the Franklin-Sterling area, Sussex County, New Jersey: Internat. Geol. Cong., 18th, London, Repts., pt. 7, p. 77-87. Pirsson, L. V., and Washington, H. S., 1907, Contributions to the geology of New Hampshire-No. III, on Red Hill, Moulton- boro: Am. Jour. Sci., 4th ser., v. 23, p. 257-276, 483-447. Platt, R. E., 1947, A little known Wyoming locality [Encamp- ment areal: Mineralogist, v. 15, no. 5, p. 227-230. Pough, F. H., 1941, Occurrence of willemite: Am. Mineralogist, v. 26, p. 92-102. Preuss, E., and Gliszezynski, S., 1951, Uber den Berylliumgehalt einiger Wavellite: Geochim. et Cosmochim. Acta, v. 1, p. 86-88. Quinn, Alonzo, 1937, Petrology of the alkaline rocks at Red Hill, New Hampshire: Geol, Soc. America Bull., v. 48, p. 878-402. 1944, Magmatic contrasts in the Winnipesaukee region, New Hampshire: Geol. Soc. America Bull., v. 55, p. 473-496. Ramberg, Hans, 1949, The facies classification of rocks-a clue to the origin of quartzo-feldspathic massifs and veins: Jour. Geology, v. 57, p. 18-54. Rankama, Kalervo, 1946, On the geochemical differentiation in the earth's crust: Comm. geol. Finlande Bull. 137. Rankama, Kalervo, and Sahama, Th. G., 1950, Geochemistry : Univ. Chicago Press. Ransome, F. L., 19012, The ore deposits of the Rico Mountains, Colorado: U. S. Geol. Survey 22d Ann. Rept., 1900-1901, pt. 2, p. 229-398. 1901b, A report on the economic geology of the Silverton quadrangle, Colorado: U. S. Geol. Survey Bull. 182. trict, Colorado: U. S. Geol. Survey Prof. Paper 75. 1913, The Turquoise copper mining district, Arizona: U. S. Geol. Survey Bull. 530-C, p. 125-184. 1922, Ore deposits of the Sierrita Mountains, Pima County, Arizona : U. S. Geol. Survey Bull. 725-J, p. 407-440. 1923, Geology of the Oatman gold district, Arizona: U. S. Geol. Survey Bull. 748. Ray, L. L., and Smith, J. F., Jr., 1941, Geology of the Moreno Valley, New Mexico: Geol. Soc. America Bull., v. 52, p. 177- 210. Raynor, G. V., 1946, Beryllium, beryllium alloys, and theoretical principles affecting alloy formation with beryllium: Royal Aeronautical Soc. Jour., v. 50, p. 890-415. 1911, Geology and ore deposits of the Breckenridge dis- 193 Read, M. C., 1903, Preliminary note upon the rare metals in the ore from the Rambler mine, Wyoming: Am. Jour. Sci., 4th ser., v. 16, p. 268. Reynolds, F. M., 1948, Occurrence of vanadium, chromium, and other unusual elements in certain coals: Soc. Chem. Indus- try [London] Jour., v. 67, p. 841-345. Rezek, A., and Tomic, K., 1942, Beryllium in Sediment des Mineral Wassers der Tempel-Quelle in Rohitsch-Saurebrunn (Untersteiermark) : Balneologe, Band 9, p. 9-13. Rickard, Forbes, 1904, Notes on tungsten deposits in Arizona: Eng. Mining Jour., v. 78, p. 263-265. Richardson, G. B., 1904, Report of a reconnaissance in Trans- Pecos Texas, north of the Texas and Pacific Railway : Texas Univ. Mineral Survey, Bull. 9. 1909, Description of the El Paso quadrangle, Texas: U. S. Geol. Survey Geol. Atlas, Folio 166. 1914, Description of the Van Horn quadrangle, Texas: U. S. Geol. Survey Geol. Atlas, Folio 194. , Rienacker, G., 1932, Detection of beryllium in minerals: Zeit- schr. anal. Chemie, Band 88, p. 29-88. Ries, Heinrich, and Bowen, W. C., 1922, Origin of the zine ores of Sussex County, N. J.: Econ. Geology, v. 17, p. 517-571. Roberts, R. J., 1943, The Rose Creek tungsten mine, Pershing County, Nevada: U. S. Geol. Survey Bull. 940-A, p. 1-14. Rodolico, Francesco, 1943, Ricerche sui constituenti minori di alcune rocce vulcanische dell'Italia central: Periodico di Mineralogia, Anno 14, p. 99-132. Rodolico, Francesco, and Pieruccini, Renzo, 1943, I1 berillio nella differenziazione del magma selagitico: Soc. Mineralog. Italiana, Rendiconti, Anno 2, p. 41-46. Russell, B., Sachs, D. C., Wattenberg, Albert, and Field, R., 1948, Yield of neutrons from photo-neutron sources: Phys. Rev., v. 78, p. 545-549. Rothrock, H. E., Johnson, C. H., and Hahn, A. D., 1946, Fluor- spar resources of New Mexico: New Mexico Bur. Mines . Bull. 21. Sahama, Th. G., 19452, Spurenelemente der Gesteine in Sudli- chen Finnisch-Lapland: Comm. Geol. Finlande, Bull. no. 135. 1945b, The chemistry of the East Fennoscandian rapakivi granites: Comm. geol. Finlande Bull. 136, p. 15-87. Sandell, E. B., 19402, Determination of small amounts of beryl- lium in silicates: Indus. and Eng. Chemistry, Anal. ed., v. 12, p. 674-675. 1940b, Morin reaction for beryllium : Indus. and Eng. Chemistry, Anal. ed., v. 12, p. 762-764. 1944, Colorimetric determination of traces of metals: New York, Interscience. 1947, Contamination of silicate samples crushed in steel mortars: Indus. Eng. Chemistry, Anal. ed., v. 19, p. 652. 1949, Determination of beryllium in silicate rocks: Anal. Chimica Acta, v. 3, p. 89-95. 1952, The beryllium content of igneous rocks: Geochim. et Cosmochim. Acta, v. 2, p. 211-216. Sandell, E. B., and Goldich, S. S., 1948, The rarer metallic con- stituents of some American igneous rocks: Jour. Geology, v. 51, p. 99-115, 167-189. Schiebold, E., 1931, Uber die Isomorphie der Feldspatminer- alien: Neues Jahrb., Beilage-Band 64A, p. 251. Schmitt, Harrison, 1935, The Central mining district, New Mexico: Am. Inst. Mining Metall. Engineers Trans., v. 115, p. 187-208. 1939, The Pewabic mine: Geol. Soc. America Bull,, v. 50, p. 777-818. 194 Schrader, F. C., 1915, Mineral deposits of the Santa Rita and Patagonia Mountains, Arizona : U. S. Geol. Survey Bull. 582. 1917, Geology and ore deposits of Mohave County, Ari- zona: Am,. Inst. Mining Metall. Engineers Trans., v. 56, p. 195-2836. Schroeder, Fritz, 1981, Spectrographische Untersuchungen an Gesteinen und Mineralien des Katzenbuckles in Odenwald : Neues Jahrb. Mineralogie Petrographie, Geologie, Beilage- Band 63, p. 215-266. Schultz, A. R., 1909, The northern part of the Rock Springs coal field, Sweetwater County, Wyoming: U. S. Geol. Sur- vey Bull. 341-B, p. 256-282. Schultz, A. R., and Cross, Whitman, 1912, Potash-bearing rocks of Leucite Hills, Sweetwater County, Wyoming : U. S. Geol. Survey Bull. 512. Secrist, M. H., 1924, Zine deposits of east Tennessee: Tenn. Dept. Education, Div. Geology Bull. 81, 165 p. Sestini, Fausto, 1888, Di alcune elemente chimici rari a tro- varsi nei vegetabli: Sta. Sperimentali Agrarie Italiane, v. 15, p. 290-296. t Shannon, E. V., 1922, Note on the cyprine from Franklin, N. J.: Am. Mineralogist, v. 7, p. 140-142. Shcherbakov, D. I., 1936, Genetic types of beryllium deposits - in the U. S. S. R.: Redkie Metally, v. 5, p. 85-41. Singewald, Q. D., 1942, Stratigraphy, structure, and mineraliza- tion in the Beaver-Tarryall area, Park County, Colorado : U. S. Geol. Survey Bull. 928-A, p. 1-44. 1951, Geology and ore deposits of the upper Blue River area, Summit County, Colorado: U. S. Geol. Survey Bull. 970, p. 1-73. Smith, F. G., 1948, Transport and deposition of the non-sul- phide vein minerals-III. Phase relations at the pegmatit- ic stage: Econ. Geology, v. 43, p. 535-546. Smith, G. O., Tower, G. W., and Emmons, S. F., 1900, Description of the Tintic special quadrangle, Utah: U. S. Geol. Survey Geol. Atlas, Folio 65. Smith, J. F., Jr., and Albritton, C. C., 1949, Sierra Blanca field trip: West Texas Geol. Soc. Guidebook no. 1, p. 95-108. Smith, J. F., Jr., and Ray, L. L., 1943, Geology of the Cimarron Range, New Mexico: Geol. Soc. America Bull., v. 54, p. 891-924. Smyth, H. D., 1945, Atomic energy for military purposes: Princeton Univ. Press, 308 p. 5 Sneddon, H. D., and Gibbs, H. L., 1947, Beneficiation of western beryl ores: U. S. Bur. Mines Rept. Inv. 4071, 18 p. Soule, J. H., 1948, West Pinos Altos zinc-lead deposits, Grant County, New Mexico: U. S. Bur. Mines Rept. Inv. 4237. Spencer, A. C., 1903, Mineral resources of the Encampment cop- per region, Wyoming: U. S. Geol. Survey Bull. 218, p. 158- 162. 1904, The copper deposits of the Encampment district, Wyoming: U. S. Geol. Survey Prof. Paper 25. Spencer, A. C., and Paige, Sidney, 1935, Geology of the Santa Rita mining area, New Mexico: U. S. Geol. Survey Bull. 859. Spencer, L. J., 1924, Euclase and platinum from diamond-wash- ings in British Guiana: Mineralog. Mag., v. 20, p. 186-192. Spencer, R. V., 1946, Exploration of the -Magnet Cove Rutile Company property, Magnet Cove area, Hot Springs County, Ark.: U. S. Bur. Mines Rept. Inv. 3900. Spurr, J. E., Garrey, G. H., and Ball, S. H., 1908, Economic geology of the Georgetown quadrangle, Colorado: U. S. Geol. Survey Prof. Paper 63. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Stephenson, E. L., 1941, Geophysicu: and geological investiga- tions of the Casper Mountain chromite deposit, Wyoming [abs.]: Washington Acad. Sci. Jour., v. 31, no. 4, p. 170. Stevens, R. E., and Carron, M. K., 1946, Determination of beryl- lium in ores, in Contributions to geochemistry, 1942-45 : U. S. Geol. Survey Bull. 950, p. 91-100. Stobbe, H. R., 1949, Petrology of volcanic rocks of northeastern New Mexico: Geol. Soc. America Bull., v. 60, p. 1041-1093. Stoll, W. C., 1945, Presence of Be and associated chemical ele- ments in wall rocks of some New England pegmatites: Econ. Geology, v. 40, p. 136-141. Stone, R. W., 1911, Geologic relation of ore deposits in the Elk- horn Mountains, Montaina : U. S. Geol. Survey Bull. 470-B, p. 75-98. Storms, W. R., 1947, Iron Mountain beryllium deposits, Sierra and Socorro Counties, New Mexico: U. S. Bur. Mines Rept. Inv. 4024. Stose, G. W., and Miser, H. D., 1922, Manganese deposits of western Virginia: Virginia Geol. Survey Bull. 23. Stoyanow, Alexander, 1942, Paleozoic paleogeography of Ari- zona: Geol. Soc. America Bull., v. 53, no. 9, p. 1255-1282. Stringham, B. F., 1942, Mineralization in the West Tintic mining district, Utah: Geol. Soc. America Bull., v. 53. p. 267-290. Strock, L. W., 19412, A new helvite locality-a possible beryllium deposit: Econ. Geology, v. 86, p. 748-751. 1941b, Geochemical data on Saratoga mineral waters- applied in deducing a new theory of origin: Am. Jour. Sci., v. 239, p. 857-898. Switzer, George, 1939, Pegmatites of Mount Antero, Colorado: Am. Mineralogist, v. 24, p. 791-809. Szabo, Josef, 1882, Helvin von Kapnik, ein fur Ungarn neues Mineral: Magyar tudom. akad., Budapest-Akad. ertesdito, ser. 3, v. 16, p. 178; abs. : Zeitschr. Kristallographie, Band 8, p. 533, 1884. Szelenyi, Tibor, 1987, Beryllium in bauxites: Magyar tudom. akad. Math. termesz ert., v. 56, p. 231-246; Chem. Abs., v. 32, p. 1616, 1938. Taylor, J. H., 1935, A contact metamorphic zone from the Little Belt Mountains, Mont.: Am. Mineralogist, v. 20, p. 120-128. Tetyaev, M. M., 1918, Les gisements de tungsten et d'etain de la region l'Onon-Borzia en Transbaikalie: [SSSR] Glavynoe geologorazvedochnoe upravlienie Izv.; Trudy; Vestnik- Materialy po obscchei i prikladnoi geologie, no. 82; Miner- alog. Abs., v. 2, p. 89-91, 1925 . Thomas, B. E., 1949, Ore deposits of the Wallapai district, Ari- zona: Econ. Geology, v. 44, p. 663-705. Tilley, C. E., 1927, Vesuvianite and grossular as products of regional metamorphism : Geol. Mag. [Great Britain], v. 64, p. 872-876. Tolmacey, Yu. M., and Filippov, A. N., 1984, Presence of rubi- dium, beryllium, gallium and strontium in nephelites: Akad. Nauk SSSR Compte Rendu (Doklady), v. 3, p. 866-869. Tolman, Carl, 1931, Quartz dikes: Am. Mineralogist, v. 16, p. 278-299. Tower, G. W., Jr., and Smith, G. O., 1899, Geology and mining industry of the Tintic district, Utah: U. S. Geol. Survey, 19th Ann. Rept., 1897-98, pt. 8, p. 601-767. Trustedt, O., 1907, Die Erzlagerstatten von Pitkaranta: Geol. Comm. Finlande Bull. 19, p. 270-271. Tschirwinsky, P. N., 1929, Beitrage zur Mineralogie Russlands III: Zeitschr. Kristallographie, Band 70, p. 249-282. Turner, H. W., 1919, Review of recent literature on tungsten de- posits of Burma: Econ. Geology, v. 14, no. 8, p. 625-639, SELECTED REFERENCES Turner, F. J., 1948, Mineralogical and structural evolution of the metamorphic rocks: Geol. Soc. America Mem. 30, 342 p. Tuttle, O. F., and Friedman, I., 1948, Liquid immiscibility in the system H«0-Na,0-8i0:: Am. Chem. Soc. Jour., v. 70, P. 919-926. Underwood, A. L., and Neuman, W. F., 1949, Color reaction of f beryllium with alkannin and napthazarin: Anal. Chemistry, v. 21, p. 1348-1852. Uzamasa, Y., 1949, Minor inorganic constituents of coals: Chem. Researches (Japan), Inorganic and analytic chemistry, v. 5, p. 1-17 ; Chem. Abs., v. 48, p. 8639, 1949. Vanderwilt, J. W., 1937, Geology and mineral deposits of the Snowmass Mountain area, Gunnison County, Colorado: U. S. Geol. Survey Bull. 884. 1938, Geology of the "Questa" molybdenite deposit, Taos County, N. Mex.: Colorado Sci. Soc. Proc., v. 13, no. 11, p. 599-643. 1947, Mineral resources of Colorado: Colorado State Mineral Resources Board, Denver. Varnes, D. J., 1944, Preliminary report on the geology of a part of the Rico Dome, Dolores County, Colorado : U. S. Geol. Survey Strategic Minerals Inv. / Vitaliano, C. J., 1944, Contact metamorphism at Rye Patch, Nevada: Geol, Soc. America Bull., v. 55, p. 921-950. Vogel, J. H., 1887, Uber die chemische Zusammensetzung des Vesuvians : Gottingen Univ. dissertation. Wadsworth, M. E., 1880, Danalite from the iron mine, Bartlett, N. H.: Boston Soc. Nat. History Proc., v. 20, p. 284-286. Wager, L. R., and Mitchell, R. L., 1943, Preliminary observa- tions on the distribution of trace elements in the rocks of the Skaergaard intrusion, Greenland: Mineralog. Mag., v. 26, p. 283-296. Waldschmidt, W. A., and Adams, J. W., 1942, The beryl-mona- zite pegmatite dike of Centennial Cone, Colorado: Colo- rado School Mines Quart., v. 37, no. 3, p. 29-38. Warren, B. E., 1929, The structure of tremolite: Zeitschr. Kris- tallographie, Band 72, p. 42-57. Warren, B. E., and Modell, D. I., 1931, The structure of vesu- vianite: Zeitschr. Kristallographie, Band 78, p. 422-482. Washburne, C. W., 1910, The Canon City coal field, Colorado : U. S. Geol. Survey Bull, 381-C, p. 341-378. Washington, H. S., 1900, Igneous complex of Magnet Cove, Ark. : Geol. Soc. America Bull., v. 11, p. 389-416. 1931, Beryllium in minerals and rocks: Am. Mineralogist, v. 16, p. 37-41. Weed, W. H., 18992, Description of the Fort Benton quadrangle, Montana: U. S. Geol. Survey Geol, Atlas, Folio 55. 1899b, Description of the Little Belt Mountains quad- rangle, Montana: U. S. Geol. Survey Geol. Atlas, Folio 56. 1901, Geology and ore deposits of the Elkhorn mining district, Jefferson County, Montana: U. S. Geol. Survey 224 Ann. Rept., pt. II, p. 399-550. Weissenborn, A. E., 1948, A new occurrence of helvite: Am. Mineralogist, v. 33, p. 648-649. 195 Wheeler, G. V., and Burkhardt, W., 1950, Semi-quantitative spectrographic analyses, in Kerr, P. F., and others, Analy- tical data on reference clay materials: Am. Petroleum Inst. Proj. 49, Prelim. Rept. no. 7, p. 71-90. White, C. E., and Lowe, C. S., 1941, Fluorescent tests for beryllium and thorium: Indus. and Eng. Chemistry, Anal ed., v. 18, p. 809-810. Wichman, F. M., 1920, The Ophir mining district : Eng. Mining Jour., v. 110, no. 12, p. 560-563. f Wickman, F. E., 1944, Some notes on the geochemistry of the elements in sedimentary rocks: Arkiv. Kemi Mineralog, Geol., Band 19B, Hafte 1, no. 2. Wilkerson, A. S., 1946, Nepheline syenite from Beemerville, Sussex County, New Jersey: Am. Mineralogist, v. 81, p. 284-287. Wilkerson, A. S., and Comeforo, J. E., 1946, New Jersey nepheline syenite: Ceramic Age, v. 48, p. 103-104. Williams, H. C., 1946, Beryllium-copper ; its uses and potentiali- ties: Steel, v. 118, no. 19, p. 88-91, 142, 144, 146. Williams, J. F., 1891, Igneous rocks of Arkansas : Arkansas Geol. Survey, Ann. Rept., 1890, v. 2. Wilson, E. D., 1927, Geology and ore deposits of the Courtland- Gleeson region, Arizona: Arizona Bur. Mines Bull. 128. 1941, Tungsten deposits of Arizona : Arizona Bur. Mines Bull. 148. 1950, Pima district, in Arizona zine and lead deposits : Arizona Bur. Mines Bull. 156, p. 39-51. Wilson, E. D., Cunningham, J. B., and Butler, G. M., 1934, Ari- zona gold mines and gold mining : Arizona Bur. Mines Bull. 137. Winchell, A. N., 1914, The mining districts of the Dillon quad- rangle, Montana and adjacent areas: U. S. Geol. Survey Bull. 574. 1951, Elements of optical mineralogy, 4th ed.-part II, Descriptions of minerals: New York, John Wiley and Sons. Wolff, J. E., 1938, Igneous rocks of the Crazy Mountains, Mon- tana: Geol. Soc. America Bull., v. 49, p. 1569-1626. Worcester, P. G., 1919, Molybdenum deposits of Colorado, with general notes on the molybdenum industry : Colorado Geol. Survey Bull. 14. Yarham, H. R., 1945, Beryllium-copper : Iron Age, v. 155, no. 17, p. 63-67. Yoder, H. S., Jr., 1950, Stability relations of grossularite: Jour. Geology, v. 58, p. 221-253. Yung, M. B., and McCaffery, R. S., 1903, The ore-deposits of the San Pedro district, New Mexico: Am. Inst. Mining Metall . Engineers Trans., v. 33, p. 350-862. Zermatten, H. L. J., 1933, A reaction for beryllium in minerals and rocks: K. Akad. Wetensch. Amsterdam, Proc., v. 86, p. 899-900. Zilbermintz, B. A., and Rusanov, A. K., 1936, The occurrence of beryllium in fossil coals: Akad. Nauk SSSR Compte rendu, new ser., v. 2, p. 27-31. Zilbermintz, B. A., and Roschkova, E. W., 1983, Zur Frage des Vorkommens von Beryllium in Vesuvianen: Centralbl. Mineralogie, 1933, Abt. A, p. 249-254. IN DEX A Page ACKNOWIOUEM@NES.L.. .._ ones f 4 Adams, J. W., section by.- 163 3, 4 Analytical methOd8, COIOFIM@ETIG. .. . . enne --- ---> 6,7 .L IC.... sou bone etch ewes s abawaank bene aon nun aind 6,7 6 7-8 ««... coulc lend cn, 00000 ee nee dunk s be on ban hotke 8 SDECHOBTADRIG..... ...... 6 VOIMIMGHTIG........_. ...... 6 Arizona, localities S&MpIGG ANd AMALYS@8. ...... 93-107 Arkansas, localities sampled and 179-181 Associated e1@MeNtS it cc ence ncn ne ~~~ 40-57 B Barylite - hve ace .. 184-185 Bertrandite P 11 Beryl, alteration 25 BeQ content y 12 concentration in Sedimentary FOCKS... 25 mineralogy... - 7, 10, 12, 25 occurrence, vein..........~- 34, 35, 36, 39, 71, 74, 97-99, 101, 106-107, 122-125, 163, 185 - 145-147 _____ ss 144-145 production...... s 2-3 Beryllium, genesis of s -se 58-59 mineralogy. 1 8-20 DrOGUCHION.L. ... 2 properties and uses. a+ 2 C California, localities sampled and 85-95 Chemistry of berylliUM, cece cece} ne -~ 8-10 SOB ank bees noe on s 26 spring water...... weathering processes.. COhrysobery1........._..._.. Coal, deposits, beryllium in.. bo 28 localities investigated, Colorado __ 161, 165, 166, 174, 176 Wyoming..........._..-... 157, 159 Color&do, localities sampled and ANAly8e8...............----~---------~- _. 159-179 ColOrIM@trIG ANALYSIS . .. cance ns 6,7 D Danalite. alteration.... #s ess 25 c 2.1... s Meve 25 occurrence................- Nei bers oe ae 30, 182 y Feldspars, analysis. ......~- a Wne ...> 14,19 Fluorimetric analysis. 6,7 Fluorite associated with helvite. See table 30-35, 40 a Garnet, analysis, ..... 14, 17, 122, 151, 186 occurrence .. 14, 122, 129, 151, 185 Genesis of beryIlUM 58-59 Gravimetric analysis...... 6 Guide to nonpegmatite deposits, 50-61 40-57 H Helvite, analysis, * oor 11 mineralogy. 10, 11, 12 occurrence, pyrometasomatic deposits.. ..... 29, 30, 34, 122-125, 129, 176, 177, 182 vein deposits. 36, 38, 39, 154 OtRET G@DOSItS, . . .... ccc 114-116 Page Hot Springs, d@DOSitS, ANALYSIS . . ... cane cece cnn nne => 39 Localities investigated, Arkansas __ 180, 181 Nevada...s...._.._....:««1- aree as bes sone ance _.... 64, 65, 69, 70 I Idocrase, analysis L-- 7,14, 17, 97, 123, 185 25, 30, 97, 123, 124, 129, 151, 182, 185 Igneous rocks, average beryllium content...... distribution of -. 22, 23, 24 foreign 10C@Iiti@8, ANALYSIS ..... .._ nnn 20-22 mode of beryllium occurrence.. localities investigated, analysis.........- Arkansas, Bryant-Bauxite area.... .. Little Rock area Magnet Cove.....................~ Colorado, Iron Hill...... Morley area.. - Ouray Peak........-~- Walsenberg area...... Montana, Gordon Butte Yoso Peak............. New Jersey, Beemerville area. New Hampshire, Red Hill.....~-- New Mexico, Raton volcanic region. Wind Mountain area. Texas, Cave Peak.......- 'Trans-Pecos Region....-- Utah, SheeprOCk 145-148 Topaz Mountain, Thoma$ RANg@.........~.------------------~- 144, 145 Wyoming, Casper Mountain.... 158 FOrt WASRAKIG 158 Halle@K CrGK 158 TFON MOURtAIML .._... eee 155-157 Leucite Hills.... 159 Investigations, purpose... 1-2 !.. nce neue 4-5 K . Kaolinite analysis.... 25, 28 L Lateritic fron ore, analysig........-...-~-- 28 LiMEStONEG, ADAIYSIS..... essense 26, 27, 139 RaWIINS 810A, cons 157 M Maine, localities sampled ANd ccna ~~~ 182 Manganese oxide ores, 27, 28 localities investigated, Golconda deposit, 64, 65 Sodaville BTB, NOVAUB . enna ones 69, 70 MetaMOTDPhit FOCKS, AMAIYSIS . . . .._... ~s 20 Mill products, .. 92, 97, 103, 105, 116, 120, 130, 172, 175, 179, 184 concentrate analysis, cassiterite 174 154 fFAAEHNItGL _... cose esen cane cece =s 184 molybdenite. monazite...~..- ZIMQ OPO.... . nece 1.0.08 % 154 197 198 INDEX Page Page Mineralogy of beryllium...) 2s. lise nas oud XL . l oni aly $20 | OFC ¢ cen- Pious reine es ceasrse aso ae 2, 3, 10, 59, 60 Minerals: See also Beryl, Chrysoberyl1, Helvite, Phenakite. Beryllium as an accessory constituent (table)....___._.....____.________ 13-15 'Ofe £- Cec rr abr es eed icine ons nea 2-4 in carbonates, calcite. ......_..__..._____.. 26, 151, 185 magnesite. .... 2. 71 P ThodooHFO#IGG.- --. -~ ne ccens nds 16 | Phenakite, rue ce «eases H, 12.17 in halides, fluotife. 116, 120, 130, 151, 174 OCOHTTONOE-- 1 c iz cece ns}. aslo s enemies eeven ae eca eo oes 98, 188 in oxides including complex metal oxides, beuxife........:......... 16, 28 Phosphate rocks, analysis yes a setae een a onto 27,154 DMOS. .,., comms nn neces To |- Properfice of n... I 2 franklinite... -- - 185 | Pyrometasomatic deposits, 29, 30, 31, 32 characteristics of beryllium-bearing depogits>-....._....... Ane 33, 34 foreign localities, analy8i8. .c . . 02000000200. % 20 helvite-danalite bearing deposits, New Hampshire.... - 182, 183 New Mexico, Carpenter district, Grant County. - 114-116 185 Iron Mountain, Sierra County...._....___..... 3 129 in phosphates, arsenates, and sulfates, apatite.... - 185 j Victorio district, Luna County. ......________. 1122-123 65, 66 other deposits, Franklin district, New Jersey - 183-185 svabite.. == 185 CO¥By (Le, 02002 ne eo cn neve noone re 179-181 An --- L..... . cn uo on o ec boar eens sacs den one savant e. 16-20 BThphibOlG§.. 0.00000. Reh 18 R 7083 | Radiometric analysis...........____________._ - 8 anthophyllite......_._. 139 8 o gamdxgting gauginuimlmf berylli s z 2 j """"""""""""""""""""""""""""""" & andstone deposits, analysis 0: HIC» Jee 5-27 $1312)? * sfafizlliimm Fort Washakie area, Wyoming. ...._...____.____.__.... i 158 Floer as'e See I docrés 6 Shale deposits, analysis of beryllium....................... - 25, 26, 27 levi 4 i Smelter products analysis of berylMUm......................_............... 154,179 cen nner not de aan e nals o 25 g pectrographic analysis sed 5 ThiCa . Gen 18, 19, 151 Suggestions for prospecting 590-60 nepheline 19,95 |_ TOA ook o SG v wo pYrOphyIIIfG.. : +22 1-1 on ini 70 m DYTORONCSLL. 4.000. .s. Cn ICT - 18, 25, 139, 151, 185 tephroite. . 185 Texas, localities sampled and analysis. See Trans-Pecos Region. FOurMaling. 1 2, 20 00002001 edu ien edie e cea al 18 | 'Trans-Pecos Region, Texas and New Mexico, localities sampled and analysis. 130-143 willemite £ 17,185 Tri-State lead-zinc district, localities Sampled. s 1 en SATII ATC 181 Af SUIAOOS » cenit ssl (concern dds ac 16 Sphalerite, ...; lo nc ds 185 U Beryllium essential .s ...o. . 10-12 "| Uses Of Dery ? 2220001 sense eld Peon eee above de cbc ens s Pocuas 2 See also Barylite, Beryl, Bertrandite, Chrysoberyl, Helvite, Phenakite. Utah, localities sampled and analysis. ..........._.._.........____... -.. 143-148 Montana, localities sampled and analy$i8.................__.____..._._..... 148-155 t y ® N Vein deposits, Beryl-bearing. See Beryl. Nevada, localities sampled and analy8i8. .........._..._......_._...__...... 63-85 Beryllium-Degrit? .. ... ... 0082002000000 nek cree: noes ««« - 85, 36 New Hampshire, localities sampled and -_ 182-183 San Franciseq distritt, - 102, 103 New Jersey, localities sampled and analysis.... -. 183-185 Helvite-bearing. - See Helvite. New Mexico, localities sampled and .. 107-130 £ypOS < 35, 36 Also see Trans-Pecos Region. Virginia, localities sampled and 185 0 w Olson, J. © :35 DY : ... 222 2 or £ us n s eL oen ane o oes n nine cen vaginal 144-145 | Wyoming, localities sampled and analysis............._.....__._____....._._._ 155-159 GEOLOGICAL SURVEY See fig. 38 10,9 NEW MExico CORNUDAS MOUNTAINS 32° O0' as ", ° L Cl a.. orero | co f a HUDSPETH| Co 12 TEXAS | ‘l ® 3 | s |‘ HUECO MOUNTAINS re | "Ne DOG MOUNTAINS 16 14 @ ’ \_ SIERRA TINAJA PROFESSIONAL PAPER 318 PLATE 1 LIST OF INTRUSIVE BODIES 1 Peak 5106 2 Hueco Tanks 3 Cerro Alto 4 Alamo Mountain 5 Flattop Mountain Oj 0 6 Little Wind Mountain o O 7 Wind Mountain w .|5 PIN TA 8 Cornudas Mountain fizm s 9 Black Mountain = O 6 10 San Antonio Mountain '/EL P1450 & L—J 2 11 Washburn Mountain x AMp 12 Chattfield Mountain | U i 13 Dog Mountains _| a 3 14 Miller Mountain t lg 17 480 15 Peak 5650 Toe 4 16 Cerro Diablo ° 00' ->» 17 Cornudas Station cARLSBAD 18 Antelope Hill 19 Sierra Prieta 20 Marble Canyon 21 Cave Peak 22 Mine Canyon 23 Granite Mountain 24 Finlay Mountains ‘IB 25 Peak 5558 26 Round Top 27 Little Blanca Mountain 28 Triple Hill 29 Sierra Blanca 19 30 Flat Mesa 31 Pinnacle Peak “SERRA PRIE TA 32 Red Chief Peak 33 Wylie Mountains j #23 INDEX MAP 31° 30 , {JSee pl. 5 New mapping by W. T. Holser, W. I. Finch, and V. R,. Wilmarth, SIERR 1948-1949. Ba--Baker, C. L., 1927. (Scale of geologic map fe 1:250, 000) {ou e} Be--Beede, J. W., 1918. (Scale of geologic map A f 1:187, 500) Lule sa NHK FINLAY MOUNTAINS | j C--Clabaugh, S. E., 1941. Geology of the north y 4/1." % § western Cornudas Mountains, N. Mex.: Texas V/‘l ‘ [0 Univ. master's thesis. (Scale of geological gages map 1:18, 000) "A* I H--Huffington, R. M., 1943. (Scale of geological 26 ‘27 2g o 0 [$1 map 1:62, 500 .' R hs y sierra sLanca e K--King, P. B., 1949. (Scale 1:150, 000) o AL 29 0 g I K--King, P. B., and Knight, J. H., 1944. Q *ig L (Scale 1:62, 500) -I 7. a » WI o F- K--K--K--King, P. B., King, R. E., and Knight, f ‘30 (0/3 LJ J. B., 1945. (Scale 1:62, 500) U « o [ea) Sierra Blanca S |3 S--A--Smith, J. F., Jr., and Albritton, C. C., T "O 1949. (Scale of geologic map 1:280, 000) i\ | T--Timm, B. C., 1941. Geology of the southern J‘ * 44/0 Cornudas Mountains, Tex. and N. Mex.: Texas Univ. master's thesis. (Scale of o geologic map 1:18, 000) '* CA Cg Z--Zapp, A. D., 1941. Geology of the northwestern ‘F/O V)‘ 80 Cornudas Mountains, N. Mex.; Texas Univ. O {é master's thesis. (Scale of geologic map £9 1:18, 000) $ Base from U. S: Geological Survey and Corps of Engineers topographic and planimetric maps, polyconic projection 1 §~ 31° 00" -- 105° 30° 15 Miles ] 105° | 33 ‘wvue MOUNTAINS 00" Compiled by W. T. Holser 104° 30 467945 0 - 59 (In pocket) INTRUSIVE IGNEOUS ROCKS OF PART OF THE TRANS-PECOS REGION, TEXAS AND NEW MEXICO PROFESSIONAL PAPER 318 PLATE 2 GEOLOGICAL SURVEY polgs & & 0 S-150-456, 457, 458 I 329-195 to 202, 205 < 0.001 to 0.026 -_ brc i 4. 329-128; 0.014] 1-inch feldspa7\ crystals 339-203; 0.001 Some bands rich in nepheline phenocrysts TRUE NORTH Macher, 2~ to 4-inch sills Marble \ y \\ ( 1 1 1 aruinn e er aerated by he ne ae od or t np oo te we NAL Prd np Ogu's hg i A.¥-+'~>Ar'+-+'4-‘+‘ E i Some Téfto 7 - inch malignite sills Hueco limestone Limestone, some altered to marble, J open line pattern; interbedded shale, mostly altered to hornfels, close line pattern IGNEOUS ROCKS iil Pegmatitic nepheline syenite Contains some eudialite f TERTIARY Malignite f- 7 grils" Granular nepheline syenite ) 455 Contact, Shaw/mg dim Dashed where approximately located Limit of outcrop so wat Strike and dip of beds . Strike and dip of foliation m Claim monument # Prospect pit amps Dump 329-605; 0.0068 Sample number; percent beryllia Geology and topography by W. T. Holser and W. I. Finch, August 1949 yp, w . : ; cerF LL RH RSF] a Nabiac s tos 44% np o 4+ up) + Gpl / 329-132; < 0.004 Pon oke . ap Lo o 4 Pp c 4 Cd Paal a i a 17 14 L Pi hpt p 4. frr + ++ > + *+ Granular nepheline syenite > + - / / Seat dot n oP ecg oP uch o f n cb dp onit <4 "A .. .- s370' x. +> tg" £7 5350 ' a sh /f (le/nes/fopé"l’ 4 £. f/Nzw + / £ 5330 '+ +9 +] R #2 Mech cr * - +246 04947 Ae od sik c, op (hue t op aie ong o o «oh ob hee Hake y St nob ropean mt ie ce (aging OTERO COUNTY, NEW MEXICO 20 0 100 Feet Lace and 1 I | 1 I Contour interval 10 feet Datum is approximate mean sea level 467945 O - 59 (In pocket) UNITED STATES DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY hess SEDMENTARY ROCKS Talus and alluvium EXPLANATION QUATERNARY y a lulls Contact, showing dip Dashed where approximately located 4 Pegmatitic float /// Marble and epidote ~-_ tactite a \ _~_ .’ ~\\ Some shale/4 PROFESSIONAL PAPER 318 PLATE 3 . e=] BLACK ROCK CLAIM (DISCONTINUED) -Some magnetite .32\9—|50;—15I-, <0.004 cam. z Hueco limestone ‘E‘ Limit of outcrop Limestone, some altered to marble, & open pattern; interbedded shale, -| * Mul mostly altered to hornfels, close Strike and dip of beds pattern 4 IGNEOUS ROCKS 1 Strike and dip of crumpled beds ===) Is i heli it *~13 Peggnnagtfsnffmz 250277; e Strike and dip of foliation CH . E Strike of vertical foliation 9 Malignite w a i Claim monument a . C3, E £ Prospect pit 329-622, 0.001 Locality sampled and number; percent beryllia Granular nepheline syenite Fine-grained nepheline syenite Jt GEOLOGIC MAP OF SOUTHERN AREA, WIND MOUNTAIN, OTERO COUNTY, NEW MEXICO 50 0 300 Feet aes ess Contour interval 20 feet Datum is approximate mean sea leve! Geology and topography by W. T. Holser and W. 1. Finch, August 1949 467945 O - 59 (In pocket) Contacts irregular and gradational PROFESSIONAL PAPER 318 PLATE 4 GEOLOGICAL SURVEY m» TRUE NORTH ~s f° Ma Cher, h wor Th 7 A; Aza} 329-135; 0.006 / 329-633;0.0063 ~ 329-632; 0.0072 GEOLOGIC MAP OF EASTERN AREA, WIND MOUNTAIN, OTERO COUNTY,NEW MEXICO Contour interval 20 feet Datum is approximate mean sea level EXPLANATION SEDIMENTARY ROCKS (2x Talus and alluvium ZZ Hueco limestone Some altered to marble IGNEOUS ROCKS Pegmatitic nepheline syenite Contains some eudialite . hi ohn me's Granular nephetine syenite Fine-grained nepheline syenite so Contact, showing dip Dashed where epproximately located Limit of outcrop _A_” Strike and dip of beds . L” Strike and dip of foliation ~4- Strike of vertical foliation _a 80 Strike and dip of joints 329-632; 0.0072 Sample number; percent beryllia Geology and topography by W. T. Holser and W. I. Finch, August 1949 250 Feet 467945 O - 59 (In pocket) GEOLOGICAL SURVEY PROFESSIONAL PAPER 318 PLATE 5 EXPLANATION SEDIMENTARY_ ROCKS Talus and alluvium Principally blocks of light rhyolite porphyry IGNEQUS ROCKS QUATERNARY Tib Light rhyolite breccia Pale orange, weathering red-brown, with angular fragments up to | meter in diameter of finely banded rhyolite and rhyolite porphyry s v at" a> T\’, 4, s lel : I n , Porphyritic granite White, with quartz and feldspar phenocrysts as much as 1 cm in diameter; includes some aplite P. 4. [s Tdb ®. t. 'Dark rhyolite breccia Tab, black, aphanitic, with angular fragments as much as 2 cm in diameter. _ Tsb, gray, silicified breccia with many quartz veins TRUE NORTH v TERTIARY APPROXIMATE MEAN DECLINATION 1951 Dark rfiyolite porphyry Black, aphanitic with 2 mm feldspar phenocrysts . _- 1*4 _> of. GV/S-ISO—450 and 451;<0.001- $- ZI 329-057, <0.004"_ f+" 329-056; <0.004 329-685; 0.0049 Light rhyolite porphyry Greenish-gray, aphanitic, with feldspar and quartz pheno- crysts; includes some andesite porphyry and some non- porphyritic felsite. _ Some dikes are younger than the light rhyolite breccia 329-686; <0.0001 +\ 329-077 to 079; 0.004 to 0.017 329-077 to 079; 0.004, dark breccia :] N320-209;< 0.001, 329-208; 0.001, 329-080 and 081; C §-150-448 and 449; 0.3 and 0.02 Some dark breccia QJ j 0 / £09 A Ss 4 1000 Feet I | Contour interval 50 feet Datum is mean sea leve! Geology and topography by W. T. Holser, W. 1. Finch, andiv. R. Wilmarth, 1948-49 GEOLOGIC MAP OF CAVE PEAK, CULBERSON COUNTY. TEXAS Hornfels garnet-idocrase types Marble Hueco limestone, includes some Bone Spring limestone on western ridge 56 Ieee Contmmng dip Dashed where approximately located 90 s<-+-- Vertical contact Indefinite contact Limit of outcrop 465 anl n Fault, showing dip 75 Vein, showing dip 90 -6-+a- Vertical vein 35 Strike and dip of beds 90 ge Strike of vertical beds Includes spurrite-merwinite, garnet-wollastonite, and Limestore, unaltered Gray to blact, clastic to marly PERMIAN White, coarse-grained gs Generalized strike and dip of crumpled beds 90 o- Generalized strike of crumpled vertical beds 55 Strike and dip of foliation Inclined shaft | al Vertical shaft ye- Portal of adit X Small prospect pit S-150-517; <0.001 Sample number; percent beryllia 467945 O - 59 (In pocket)