COLUMBH Ministry of Employment and Lnvestnlent Energy and Minerals Division Geological Survey Branch

Home , Fluorapatite, Marks Head Formation, Monkman Pass, Mount Brewster, Mount Proctor, Phosphorite

BFUTISH .. COLUMBH Ministry of Employment and lnvestnlent Energy and Minerals Division Geological Survey Branch

By S. Butrenchuk, P.Geo

BULLETIN 98 Canadian Cataloguing in Publication Data Buuenchuk, S.B. Phosphate deposits in British Columbia

(Bulletin ;98)

Issued by Geological Survey Branch. Includes bibliographical refeerences :p. ISBN 0-7726-2895-5 VICTORIA BRITISH COLUMBIA 1. Phosphate rock - British Columbia. 2. Geology, CANADA Economic - British Columbia. 1. British Columbia. Ministry of Employment and Investment. 11. British AUGUST 1996 Columbia. Geological Survey Branch. 111. Title. IV. Series: Bulletin (British Columbia. Minislryof Employment and Investment) ;98. Field research for lhispublication was camicd out during the period1986 to 1987. TN914.C32B74 1996 553.6'4'09711 C96-.960152-2 ABSTRACT

Phosphate is an abundant commodity worldwide and is This study discusses in detail the petrographical and produced in over 29 countries. While there is currently an chemical makeup of the sedimentary phosphate deposits, oversupply analysts believe that international bade patterns especially how they relate to beneficiation. A comprehen- will change. Canada’s traditional sources of importedphos- sive classification based on chemical and mineralogical pa- phate rock are predicted to decline and new sources may rameters is proposed for British Columbia phosphate have to be found. Thisstudy assesses the resource potential deposits. The trace element content of these deposits is also of phosphate deposits in British Columbia and comments described. Uranium, fluorine, yttrium and rare-earth metals on their economic viability. may be recoverable. Sedimentary phosphate deposits occur in 14 strati- Sedimentary phosphate was deposited in a shdf to bas- graphic units in rocks ranging in age from Cambrian to inal environment. Nodular phosphates are common and Lower Jurassic. Deposits of Triassic and Jurassic age offer characterize deposition in shallow waters while thepelletal the best potential for future development. Beneficiation varieties were deposited in a deeper water, more reducing problems and high cost mining must be overcome before environment. Many of the deposits occur above unconfor- these deposits are considered economic. A large resource is mities; better grade deposits are associated, transgressive present at the Aley carbonatite where phosphate could con- events where upwelling currents allowed phosphate depo- ceivably be produced as a byproduct from its niobium pro- sition to take place. duction.

Bulletin 98 iii - ." ~~ ~

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_- iv Geological Survey Branch Ministry of Employment and h vestment

TABLE OF CONTIENTS

CHAPTER 1 Sulphur Mountain Formation ...... 34 INTRODUCTION ...... I Toad Formation ...... 36 2 Fcmic Formation 38 OverviewFormation ofPhosphateSupply Fcmic andDemand ...... 2 ...... Scope of Work ...... 3 Acknowledgments ...... 5 CHAPTER 5 GEOCHEMISTRY ...... 41 C HAPT ER 2 Major Element Geochcmislty Element Major 2 CHAPTER ...... 41 PHOSPHATE DEPOSITSOF THENORTH AMERICANGeochemistry Element Trace ...... 41 CORDILLERA ...... 7 CHAPTER 6 FormationPhosphateof Deposits ...... 8 OF PHOSPHATE LOCALITIES ...... 45 Classification of SedimentaryPhosphate Deposits ... 9 Weathering of PhosphateDeposits ...... 9 PhosphateLocalities in the FernicBasin ...... 45 Forsyth CreekForsyth - LakesConnor ...... 45 CHAPTER 3 Macdonald Thrust Fault ...... 47 STRATIGRAPHYOF SEDIMENTARYPHOSPHATE Ski-HillFemic ...... 48 D EPOSITS INBRITISH COLUMBIAINBRITISHDEPOSITS ...... 13 Weigert Crcck ...... 48 Nordstrum Crcek 51 RegionalStratigraphy 13 ...... LineCreck ...... 51 PhosphateDeposition ...... 16 crow ...... 52 Cambro-OrdovicianPhosphate ...... 16 AlexanderCreek - Highway3 ...... 53 UpperCambrian 16 ...... Marten ...... 54 KechikaFormation ...... 16 SummitLakc ...... 54 Road River Formation ...... 17 Lizard ...... 54 Devon-MississippianPhosphate ...... 17 Mutz Creek and Uooer.. Mutz Creek ...... 55 ExshawFormation ...... 17 Fairy Crcek ...... 55 PennsylvanianPhosphate ...... 18 Island Lake ...... 55 Tunnel Mountain Formation 18 ...... Harllcy Lake ...... 55 Xananaskis Formation Xananaskis 18 ...... LladncrCrcck ...... 56 Permian Phosphatc: The Ishbcl Group and Correlative Abby ...... 56 RocksinNortheaslemBritishColumbia ...... 18 BingayCrcck ...... 56 Johnston Canyon Formation 19 Formation Canyon Johnston ...... ElkfordSki-Hill 56 Formation 21 Telford Formation ...... FordingRiver 57 Ross Creek Formation 21 ...... BarncsLake ...... 58 RangerCanyon Formation 21 ...... Lodgepole ...... 58 Belcourt Formation 23 Formation Belcourt ...... Lodge 58 M owitch Formation 23 Formation Mowitch ...... Zip 58 KindleFormation 23 ...... CabinCreek 58 FanlasqueFormation 23 ...... SheepMountain 60 Belloy Formation 23 ...... Norlh SulphurCreek ...... 61 TriassicPhosphate 23 ...... Todhunter ...... 61 SulphurMountain Formation ...... 27 AlexandcrCreek North 61 Vega-PhrosoMember 27 ...... Phosphate Localitiesin Northeastern WhistlerMcmber 27 ...... British Columbia ...... 61 Llama Member 28 Member Llama ...... McosinMountain 61 GraylingFormation 28 ...... Wapiti Lake 62 Toad Formation 28 ...... MountPalsson ...... WhitehorseFormation 32 64 ...... BakerCrcck ...... 65 TriassicSubsurface Deposits 32 ...... Lcmoray 65 JurassicPhosphate 32 ...... 65 Ludington Mount ...... FemieFormation ...... North 32 Pass Lauricr ...... 65 R ichards Creek 67 Creek Richards ...... CHAPTER 4 Tetsa Rivcr .Alaska PETROGRAPHY AND MINERALOGY OFSEDIMENTARY Highway ...... 69 PHOSPHATEBRITISHCOLUMBIA IN ...... 33 SummitLake ...... 69 Kechika FormationKechika69 ...... Peak 33 Grey ...... Road River Formation 33 Formation River Road ...... Carbonatites ...... 69 Exshaw Formation 33 Aley 33 Formation Exshaw ...... 71 Ishbel Group 33 Group Ishbel ...... Verity ...... 71

Bulletin 98 V British Columbia __

Ren(Ratchford Creek) ...... 71 14. Rcsampling resultsof the Abby and Highway3 Gap 72 Three Valley Gap ...... localities ...... 122 MiscellaneousOccurrencesPhosphate74 ...... Quesnel Area 74 Area Quesnel ...... 15. Major and trace element analyses.AIcy G randuc Tailings Granduc ...... 74 carbonatite ...... 123 Iron Mask Batholith ...... 14 16 .Analytical results forcarbonatites sampled ...... 123 FrancoisLake Asphaltum ...... 74 17. Sample locations and results for the Quesnel area.... 124 CHAPTER 7 18. Major elemcnt analyses. Quesnel area...... 124 BENEFICIATION AND PROCESSINGOF PHOSPHATEROCK ...... 75 19. Minor element analyses. Quesnel area...... 125 Beneficiation of British Columbia 20 .Mineralogical cornposition of phosphate. Whistler PhosphoriteRock ..... 77 member of the Sulphur Mountain Formation ...... 125 21 .Mineralogical composition ofphosphate. Fernie CHAPTER 8 Formation 126 RESOURCE POTENTIAL OF ...... SEDIMENTARY PHOSPHATE DEPOSITSIN TABLES BRITISH COLUMBIA ...... 85 1. Canada. phosphate fertilizcr plants (from Barry. 1986) . 4 CambrianOccurrences ...... 85 ExshawFormation ...... 86 2. Stratigraphy of phosphate-hearing formationsin PermianDeposits ...... 86 southeasternBritish Columbia ...... 14 Johnston Canyon Formation 86 ...... 3. Stratigraphy of phosphate-bearing formationsin RossCreek Formation ...... 87 Ranger Canyon Formation ...... 87 northeasternBritish Columbia ...... 15 Triassic Deposits ...... 88 4 . Qualitative mineral abundanccs in the Permian Subsurface Triassic Deposits...... 89 phosphatcs ...... 36 Fernie Formalion ...... 89 5. Qualitative abundancesof minerals in the Whistler CHAPTER 9 mcmber of the Sulphur Mountain Formation...... 36 SUMMARYAND CONCLUSIONS ...... 93 6. Qualitativc mineralabunrlances in the Toad Formation Cambrian ...... 93 phosphatc rocks ...... 38 Mississippian ...... 93 7 . Qualitativc abundanceof minerals presentin the basal Permian 93 ...... Ferniephosphatc 40 Triassic ...... 93 ...... Jurassic ...... 93 8. Averagc trace elcmcnt contentin phosphate rocks sampled in this study and average values obtainedby REFERENCES ...... 95 Gulbrandsen(1966)andAltschnler(1980) ...... 42 9 FIP205 ratios for phosphate-bearing formationsin GLOSSARY OFTERMINOLOGY USEDIN . THISREPORT ...... 99 BritishColumbia ...... 42 IO. Analytical results. Crow deposit ...... 54 APPENDICES 11. Analytical results. Fernic phosphorite. Cabin Creek 1. Calculations uscdto dctcrmine mincralogical composition area ...... 60 usedintheclassificationofphosphate rocks...... 103 12 . Phosphate specifications reuiredby fcnilizer plants 2 .Major elements, Kechikaand Road River formations . . 104 (Kouloheris. 1977) ...... 75 3 . Major elements. Permian phosphates ...... 104 13 .Effects of impurities in the manufacture of filter-grade 4 . Major elements. Triassic phosphates...... 105 wet processphosphoric acid ...... 76 5.Major elements. Fernie phosphate (Jurassic) ...... 105 14. Textural and compositional featuresof Ishhel Group phosphatcs ...... 78 6. Trace elements. Kechika and Road River formatiom. . 106 15 .Textural and compositional featurcsof the Whistler 7. Trace elements, Permian phosphates...... 106 membcrphosphatcs ...... 79 8.Trace elements. Triassic phosphates...... 107 16. Textural and compositional featuresof the Fernie 9. Trace elements, Fcrnie phosphate (Jurassic)...... 108 phosphate ...... 81 10.Sample locations and results from southeastern 17 .Texturaland Compositional features of the Toad BritishColumbia ...... 109 Formation phosphates...... 82 11. Sample locations and results from northeastern 18. Resourcepotcntialfor Permian phosphates ...... 85 BritishColumbia ...... 119 19 .Resourcepotential forTriassic phosphates ...... 86 12 .Trace elements. Wapiti Lake (Legun. 1985) ...... 121 20 . Resourcc potential for the Basal Femie phosphate.... 86 13 . Major oxides. Wapiti lake (Legun. 1985) ...... 122

. vi Geological Survey 6 ranch Ministgv of Employmenr and luveslnlenf

F'IGURES 24. Stratigraphic corrclationof phosphate-bearing strah 1. World distribution of identified phosphate resources in the Triassic of northeastern British Columbia , . , . , 30 expressed in termsof commercial product (modified 25. Stratigraphic position, thickness and correlationof fromSlansky, 1986) . . . . . , . . . . . , . . . , . . . . . 1 phosphate-bearing strata on surface andin the subsurface, 2. World productionofphosphaterock, 1970-1987 . , . . . , 2 Halfway River - Trutch map sheets (94B and 94G) , . , . 31 3. Sources of imported phosphate rock for Westem 26. Correlation between uranium and phosphate for Pelmian, Canada,early 1980s (from Werner, 1982) ...... 2 Whistler member and Fernie Formation phosphates . . , 43 4. Canadian imports of phosphate rock, 1965-1986 ...... 3 27. Correlation bctweenyttrium and phosphate for Pennian, Whistler member and Fernie Formation phosphates . , . 43 5. Locationof study area ...... , 5 28. Correlation between lanthanum and phosphale for 6. Distribution of phosphate depositsin the North Permian, Whistler member and Fernie Formation AmericanCordillera ...... , . . . . , 7 phosphates ...... , . . . . , . . . . , , 44 7. Proposed classification for phosphate depositsin 29. Stratigraphicsection 62, ForsythCreek . . , . , , . . . , 45 BritishColumbia. . . . , . . , . . . . , . , . . . , . , . 10 30. Stratigraphic section 63, Forsyth Creek . . . , . . . . . , 46 8. Compositional classificationof phosphate-bearing strata of the Permian (after Mabie and Hess, 1964) . . . . , . . 10 31. Stratigraphic correlationof phosphate-bearing strata, Johnston Canyon Formation, Fernie ski-hill- Cabir 9. Compositional classificationof phosphate-bearing strata Creek area ...... , ...... , . 47 for the Toad Formation (after Mabie and Hess, 1964) , . 10 32. Stratigraphic section 8, Fernieski-hill ...... 49 10. Compositional classificationof the Whistler member phosphate based onthe three-component systcm: 33. Location of phosphatc horizon in the Line Creek area , . 51 fluorapatite-quartz-carbonate . , . . . , . . . . . , . . . 11 34. Stratigraphic Scction 70, MountLync ...... 51 11. Compositional classificationof the basal Femic 35. Cross-sections through Fcrnie phosphate,West phosphate based on the three-component system: LineCreek . . , , . . . , . , , . , , , . . . , , . . . , . 52 fluorapatite-quartz-carbonate , . . . . . , . , . , . , . , 11 36. Cross-section through the Crow deposit 12. Classification of phosphate deposits accordingeo their (from Tclfer, 1933) ...... , . . . . , . . 53 organic and iron content (after Mabie and 37. Stratigraphic section3, Highway 3 roadcut, Hess, 1964) . . . . , . . . . , . , . . . , . . . . , . , . 11 approximately 8 kilometreseast of Michel , . . . . , . . 53 13. Distribution of Kechika Formalion and phosphate 38. Stratigraphic section31, Alexander Creek at deposits in the Grey Peak - Mount Sheffield area . . . . . 16 Highway 3 ...... 54 14. Phosphate deposits in the Fernie Basin ...... , in pocker 39. StraJigraphicsection 13, AbbyRidge , . . . . , . . . , , 56 15. Stratigraphic correlationof Pennsylvanian-Pcrmian 40. Stratigraphicsection 14, BingayCreek . . . . 56 strata and phosphate horizons inthe North American ...... Cordillera (modified from McCrossan andGlaistcr, 41. Stratigraphicsection 80, Elkfordski-hill ...... , , . 57 1964, Bambereral, 1968: MacDonald, 1985) , 19 . . . . . 42. Stratigraphicsection 6, FordingRiver , . . . , , , . . . 57 16. Distribution of phosphate-bearing stratain the 43. Geology and phosphate depositsin the Cabin Monkrnan Pass- Sukunka River area Creek area ...... , ...... 59 (931 and 93P) ...... , . , . . 24 44. Stratigraphic section 38, Cabin Creek . . . . . , . . . . . 59 17. Phosphate depositsin the Mackenzie map area (930) ...... 25 45. Section 87-6, Meosin Mountain north . . . , . , . . . . . 61 18. Phosphate deposits inthe Halfway River- Trntch 46. Section 87-7, MeosinMountain south . . , . . . . , . , 62 area (94B and 94G) . . . . . , . . . . . , . . . , . inpockef 47. Gcology of the Wapiti Lakc area (modified from 19. Phosphate depositsin the southwest cornerof the Fort Heffernan, 1980; LegunandElkins, 1986) ...... 63 Nelsonmap area (94J) . , , . , . , . . . , , . , . , . , . 26 48. Section SB87-34, MountLudington . . . , . , . . . . , 65 20. Geology and phosphate depositsin the Tetsa River 49. Section SB87-36, LaurierPass north . . . , , , . . . , . 66 area (94W9) . . . . , . . . . , . . . . , . , . . . , , . . 27 SO. Scction SB87-36(3), Laurier Passnorth (measured on 21. Distribution of Triassic stratain northeastern British west limb of anticline approximately60 metres Columbia...... , ...... 28 upsection fromSection SB87-36) , . , . , . . . , . , . . 66 22. Correlation between Triassic formations and members 51. Section SB87-37, RichardsCreek . , . . . . . , . . , . . 68 of surface and subsurface areas of British Columbia 52. Comparative grades of sedimentaly and igneous andAlberta (modified fromGibson, 1975) . . ~ , . , . . 29 phosphate ores and marketable products (from Notholt

23. Paleogeographic map of the Early Triassic (aftcr andHighley, 1986) ...... ~ , . . . . , . . 70 McCrossan and Glaistcr, 1964) ...... , . . . . . 29

Bullerin 98 vi; 53. Map showinglocations of phosphate-bearing member of the Sulphur Mountain Formation, Wapiti carbonatites (modified from Pell, 1987) ...... 71 Lake ...... 36 54. Geological map of the Aley carbonatite and sample 12. Photomircograph (40x1 of pelletal phosphorite from the locations(from Mader, 1987) ...... 71 Whistler member of the Sulphur Mountain Formationat 55. Blue River area. Map showing carbonatitelocatilities Meosin Mountain. Pellets (black), encased pellet[EP) ard (fromPell, 1985) ...... 72 nucleated pellet (NP) occur ina carbonate (Cc)-richmatrix ...... 37 56. Geology and phosphate occurrences in the Cariboo Lake-SpectacleLakesarea(93A114and93W3) .... 73 13. Photomicrograph (40x) showinga phosphate grain(P) irl calcareous siltstone (cross-nicols) from the Toad 57. The different methods of treating phosphate rock .... 75 Formation,Burnt River area ...... 37 58. Resource potential for Permian phosphates, 14. Photomicrograph(100~) in plain polarized light of southeasternBritish Columbia ...... 87 pelletal phosphoritc from thc Fcrnie Formation- Crow 59. Resource potential for Permian phosphates, deposit. Scmi-compact pellets occur ina matrix of northeasternBritish Columbia ...... 88 quartz,calcite and minorclay and mica , . , . , , . . 38 60. Resource potential for Triassic phosphates, northeastern 15. Photomicrograph (40x) in plain polarized light of BritishColumbia ...... 88 pelletal phosphorite from the Fernie Formation located at the Lizard dcposit. Pellets (P) and nucleated pellets 61. Stratigraphic correlation of the basal Fernie phosphate (P)are present in a dominantlycalcite (Cc) matrix , 39 in southeastern British Columbia...... 89 . 16. Photomicrograph (40x)of pelletal phosphorite in Ihe 62. Resource potential for theFernie phosphate, southeastern Fernie Formation - Abby locality. Phosphate pellets BritishColumbia . . , . . , . , . . , . , . , . , . . , . 90 (brown) occur in a quartz-rich matrix. Rare pelletis 63. Total formational apatite, basal phosphate horizon, nucleated(NP) ...... 39 FernieFormation ...... 91 17. View looking north along contact between Pcrmian PHOTOS Ranger Canyon Formation (RC) and Triassic Sulphur 1. Section through Upper Kechika Formation (K) and Mountain Formation (TSR) north of ForsythCreclc. Lower Road River Formation (RR) near Grey Peak ... 17 Phosphate-bearing siltstone (P) occurs along the uppcr contact of beddedchert ...... 45 2. Phosphate laminae (blue-black) ina sandstone bcd, TelfordFormation, Telford Creek ...... 20 18. Phosphate nodules (black) ina 1-metre-thick siltstone bed overlying chertat the top of the Ranger Canyon 3. Phosphatic coquinoid bed (blue) in Telford Formation, Formation in the Connor Lakes area north of TelfordCreek ...... 20 ForsythCrcck ...... 46 4. Phosphate nodules ina calcareous siltstone-coquinoid 19. Phosphate nodules and intraclasts in siltstoneof the sequence of the Ross Creek Formation north of JohnstonCanyon Formation, Mount Broadwood ... 48 SulphurCreek ...... 21 20. Phosphorite bed from the topof the Ranger Canyon 5. Basal conglomerate with phosphate cement (PC) and Formation,Fernie ski-hill ...... 48 phosphate pebbles (P) in the Ranger Creek Formation, 21. Photomicrograph (40x) of pelletal phosphorite from the CabinCreek area ...... 22 Johnston Canyon Formation, Weigert Creek. Phosphate 6. White-weathering phosphate nodulesin a siltstone from pellets (P) and nuclcatcd pcllcts(NP) occur in a calcite the Rangcr Canyon Formation, Cabin Creek area .... 22 (Cc) -quartz (Q)matrix ...... 50 7. Photomicrograph (40x) showing phosphatic oolites and 22. Pelletal phosphorite from the Johnston Canyon broken phoscrete layers from the Kechika Formation, Formation, headwatersofNordstromCreek ...... 50 GreyPeak ...... 33 23. Photomicrograph (40x) of pelletal phosphorite, basal 8. Photomicrograph (40x) showing phosphate pellets (P) and Fernie Formation, Mount Lyne locality. Phosphate pellets phosphate cement (PC) ina quartz-rich (Q)siltstone from (P) and nucleated pellets (NP) witha compact tcxturc the Johnston Canyon Formation, Mount Broadwood . . 34 occur in a quartz (Q)matrix ...... 52 9. Photomicrograph (40x) of phosphate containing phosphate 24. Phosphate nodules (white) ina brownish weathering sand- pellets (dark brown), quartz grains (white) andshe1 stone, Rangcr Canyon Formation, Upper Mutz Creek , 55 material from the Ishbel Group, Crowsnest Pass area . . 35 25. Hand spccimcnof basal Fernie phosphorite, Lodge 10. Photomicrograph (40x) of disseminated phosphate pellets phosphate occurrence. Irregular-shaped phosphate (P) in a quartz (Q)- calcite (Cc) matrix in the basal nodulesoccur in a pcllctalphosphate matrix , , , , , , 57 Johnston Canyon Formation from the Fenster 26. Photomicrograph (40x) of pcllctal phosphorite from the Creek area...... 35 FernieFormation, Cabin Creek area ...... 60 11. Photomicrograph (40x) of pelletal (P) and oolitic(0) phosphate in a quartzose matrix from the Whistler

viii Geological Survey Branch .- Minisky of Employment und Livestmen1

27. Stratigraphicsection through Vega-Phroso (VP), 31. Section through the Toad Formation(T) and lowerportion Whistler (W)and Llama (L) membersof thc Sulphur of the Ludington Formation (LUD). Hatched linem:aks the Mountain Formation south of Mwsin Monntai ...... 62 change from weakly carbonaccous-phosphate sediments 28. Folded Mississippian (MR), Permian(P) and Triassic to morc calcarcous .nonphosphatic sediments ...... 67 ega-Phroso (VP) and Whistler (W) memberstrata in thc 32. Phosphatic nodules anda solitary calcareous concretion Wapiti Lake area ...... 64 in siltstone of the Toad Formation from a localityncnh 29. Phosphate nodules (blue) in a sandstone athcd top of thc of Laurier Pass ...... 67 PermianMowitchFomation,WapitiLakearea . . , . , 64 33. Microcrystallinc coatingof phosphate (blue) around 30. Photomicrograph (40x) of phosphatic limestone, Lemoray. nodular limcstonc of thc Kechika Formation, Phosphate pellets (black) are dispersedin a carbonate-rich GreyPeak area ...... 70 matrix. Some chert (lowerIcft) and quartz are also 34. Photomicrograph under cross-nicols (40x) of subrounded present ...... 66 apatite (Ap) crystals disseminatedin a carbonate matrix, Aleycarbonatitc ...... 72

CHAPTER 1 INTRODUCTl[ON

Phosphorus is essential to all forms of animal life and rine phosphate deposits generally contain 50 to :LOO parts together with niotrogen and potassium is necessary for plant per million uranium while igneous deposits usually have a growth. Plants derivethese elements from the soil, a process lower uranium content. Concentrations of rare earthsvary that leads to the impoverishment of such vital components. considerably. Values range from a few pats per rrillion for While some of this loss may he replenished by natural proc- deposits in Florida to 1% for the Maikop and Mangyshlak esses the use of chemical fertilizers is the most effective deposits in the Soviet Union (Slansky, 1986). means of restoring these nutients to the soil. Phosphate rock Phosphate reserves worldwide are sufficient tcl last well is the most suitable source of raw material in the manufac- into the next century. The estimated resource isbelieved to ture of phosphate fertilizers. be inthe range I28 billion tonnes of which 69 billion tonnes The average phosphorus content in the ea.rth's crust is can be classified as reserves (Cathcart, 1983). Whileworld- estimated to be 0.23% P205. Igneous rocks contain an av- wide resources may be substantial, approximalely two- erage of 0.16 to0.43% P205 while sedimentary rocks con- thirds of known resources are contained in carbonate rich tain between 0.03 and 0.17% P205. Shales generally have deposits for which satisfactory beneficiation technology is the highest phosphate content. Most phosphorus occurs in not yet available on a commercial scale (Notholt and minerals of the apatite group. The structure of apatite is such Highley, 1986). that carbonate, vanadate, arsenate and sulphate may substi- Phosphate is presently produced in 29 countries with tute forphosphate and sodium, strontium, uranium, thorium the majorproducing centres and those with potentisl forpro- and rare earth elementsmay substitute forcalcium. Because duction shown in Figure 1. The United States, Morocco and of this capacity for substitution, phosphate deposits very the Soviet Union account for 70% ofthis productic n. World often represent a significant resource for these metals, in production figures for the period 1970 to 1987 areihown in particular, uranium, yttrium and the rare earth elements. Ma- Figure2,Productionofphosphatein 1987was 145.1 million

Figure 1. World distributionof identified phosphate resources expressedin terms of commercial product (modified from Slansky, 1986). Approximately 80% of phosphate production is from Im- ded sedimentary rocks and most of the balanceis from alkaline igneous rocks or carbonatites. The fertilizer indwtry consumes approximately 95% ofphosphate rockproduction while chemicals, refractories, pharmaceuticals and lood processing account for the remaining 5% (Emigh, 1983). Although Canada has substantial phosphate depcsits, none are economical at the present time and therefore imports all of the phosphate rock. The United States is the major source with Florida supplying 70% of Canada's imports and the westernUnitedStatessupplying theremainiug30%. Florida supplies 45% of western Canada's fertilizer nseds while the remaining 55% is imported from Utah, Idahc and Montana (Figure 3). In recent years Canada has begur im- porting phosphate rock from Morocco. Fertilizer plants in British Columbia presently import all of their feedstock from Montana. In 1986 the annual capacity of fertilizer plants in western Canada was 724 OOO tonnes (Table I), of which, the greatest capacity was inAlberta. At present I here is only a single fertilizerplant in the province. It is located at Trail and operated by Cominco Limited. Figure 2. World production of phosphate rock, 1970-1987.

tonnes, a decline of approximately 5% from the previous year. World production figures for theperiod 1970 to 1987 are shown in Figure 2.

OVERVIEW OF PHOSPHATE SUPPLY AND DEMAND During the 1970s and early 1980s there was a suhstan- tial increase in the production and consumption of phosphate. However, since 1980 world supply capability has exceededdemand.Asaresultthephosphatefertilizcrindus- try is currently in oversupply, a situation that is expected to continue until at least 1990. Future annual growth rates of phosphate consumed worldwide will he 3% in the fertilizer industry and 2% in the non-fertilizer sector. The long term outlook is for continuedgrowth, if for no other reason than an increasing world population. By 1995 world consumption of phosphate rock is estimated to be 180 million tonnes and by the year 2000 it isestimated to be198 million tonnes per year (Lavers, 1986). Demand will be greatest in developing countries, especially in southeast Asia. The present oversupply to the fertilizer industry is expected to end by 1990 when markets for phosphate rock should move to a more balanced position. Present trends are toward the mining of lower grade material and for exporting countriesto treat their own rock \ \..- -.J and to export products with higher added value. Imports of i \ G",. phosphate rock will he increasingly limited to those coun- hies that have an adequatesupply of sulphuric acid at com- petitive prices (Lavers, 1986) as large quantities of this acid are used to treat phosphate mkto producephosphoric acid. Canada has a plentiful supply of both sulphuric acid and sulphur and therefore isin a good position with respect to the importation of unprocessed phosphate rock. \ \, BAJ~CALIFORNIA Phosphate is pror!osed from threesources: marine sedi- \ __ mentary rocks, igneous apatite(carbonatites and related al- Figure 3. Sources of imported phosphate rock forwestern kaline intrusions) and guano-derived deposits. Canada, early 1980s (from Werner, 1982).

2 Geological Survey llranch Ministry of Employment und 111vestment

The upward trend of Canadian imports of phosphate California. Christie (1981) suggested that it would cost Ca- rock for the period 1965 to 1986 (thelast year for which data nadian $73 per tonne to deliver this material to Calgary. is available)is illustrated by Figure 4. In 1985 Canada im- Prices approaching the C$70 to C$80 range could lnake de- ported 2.64 million tonnes of phosphate rock (Barry, 1986). posits in Canada economic (Barry 1987). Imports declined again in 1986 to2.35 million tonnes. This Byproducts that may be recovered from theptocessing downward trend is notexpected to continue. Energy, Mines of phosphate rock include uranium, vanadium, fluorine and and Resources, Canada predicts that there will be an in- rare earth elements. Uranium has the best potentid for by- crease in demand but prices will not rise substantially until product recovery but is generally only recovered at a very at least 1990-92(Barry, 1987). Imports from Florida, Can- few plants. In Canada it is onlyrecovered in a single plant ada's traditional supplier, are expected to decrease because inAlberta.Wor1dproductionofuraniumisforcastedtomeet of decreased production resulting from higher mining costs demand until 1995 when production capability from known related to lower grade depositsand environmental concerns. sources (including phosphate) will begin to decline and be While there are sufficientreserves in the Phosplroria Forma- overtaken by world demand (MacDonald, 1987). tion in the western United States to take up the slack, many Vanadium is used inthe iron and steel industrq but little deposits are folded and faulted and notamenable toconven- is produced in Canada. This is the only metal that is cur- tional mining methods (Cathcart, 1983). Increased produc- rently being recovered as a byproduct of phosphate extrac- tion from the western United States will be required to offset tion in the United States. Presently world prtlduction increased consumption in the United States and a decrease exceeds demand, a situation which is expected to ,continue. in production from Florida. In mid 1988 Idaho's phosphate Future market potential is predicted to increase by approxi- production was operating at capacity. If Canada is unable to matley 2.9% until the year 2000 (Kuck, 1983). obtain its phosphate requirements from current sources, it will have to look for new suppliers or produce phosphate Fluorine is used in the chemical, ceramics and steel in- rock from within its own borders. In response to this antici- dustries and in the refining of uranium ores. Much of Can- pated needto locate its own phosphate deposits studies were ada's fluorspar requirements are imported from Mexico. initiated by Energy, Mines and Resources, Canada and by Fluorine which canbe recovered from phosphate a!: fluosilic the provincial government of Alberta (MacDonald, 1987) acid is present in all of British Columbia's sedimentary to assess the resource potential of phosphate in Canada and phosphate deposits. Only modest growth is forca;t for this Alberta respectively. Similarly, in 1986, British Columbia commodity. also began an assessment of its phosphate potential, the re- A variety of rare earth metals and yttriumoccur in sedi- sults of which are presented in this report. mentary phosphate deposits. Those in British Columbia are In 1983 the average price paid by Canadian fertilizer no exception. Rare-earth growth in the United States is for- plants for phosphate rocks imported to Canada was C$75 cast tobe less than 3% while in Japan demand fo: yttrium, (Prud'homme and Francis, 1987). Since that time prices lanthanum, cerium and europium is expected to ir~creaseat have decreased dramatically. Current prices for phosphate the rate of 13 % compounded annually until the y-ar 2000. rock are approximately US$U.SO f.o.b. vessel Tampa. The The actual growth rate for yttrium in Japan in the past few cost to Canadian fertilizer plants is actually higher once years has been 35 % (King, 1986). At the present time world freight costs are included. These prices are expected to re- consumption for yttrium is growing at a rate of 11) to 1'7 % main stable until the end of the 1980s and then rise to per annum.In 1986 the price of yttrium (99.99% purity) was US$45.00 per tonnein 1995 (basis 70% bone phosphate of U.S. $52.50 per kilogram. At the end of 1986 prices force- lime). A potential source of phosphate rock is from Baja rium were between US$21.00 and27.00 and for I;mthanum they were between US$27.50 and 45.00 (King, 1986). Yt- trium, lanthanum and cerium areused as dilutents'nnuclear reactors. Rare earth elements are also used in magnetic materials, phosphors, neutron capture applications, glass, ceramics and other uses (King, 1986).

SCOPE OF WORK Sedimentary phosphate was first discovered in Canada in 1915 near Banff in rocks of Permian age. In 1925 W.D. Burgess and L. Telfer discovered phosphate in Jurassic rocks in the Crowsnest Pass area. Since the earl:/ work of Telfer (1933) several companies that include Cominco L,im- ited, Esso Resources, Crowsnest Industries Limited and First Nuclear Corporation have conducted exphation in southeastern British Columbia. Cominco Limited con- stmcted adits at the Crow, Lizard andMarten properties and completed beneficiation tests but none went int.3 production. Metallurgical studies were also done on phosphate from the Line Creek area. With the decline of .?hosphate Figure 4. Canadian imports of phosphate rock, 1965-1986. prices in the early 1980's exploration activity declined. At

- Bulletin 98 3 British Columbia -

~~ TABLE 1 CANADA, PHOSPHATE FERTILIZER PLANTS (From Barry, 1987)

PrincipalSource of Basisfor H2S04 Plant Annual End Phosphate End Annual Plant Supyly for Company Location Capacity Products Rock Fertilizer Plalts ”- (tonnes P,OJ equivalent) EASTERN CANADA

Belledune Fertilizer Belledune, 150 000 am ph Florida SO2 smelter gas Div. ofNoranda Inc. N.B. C.I.L. Inc. CouNight, 90 000’ am ph Florida SO2 smelter gas, Onf, pyrrhotite rozst 240 000 and waste ac d WESTERN CANADA

Cominco Ltd. Kimberley, 86 700’ am ph Montana SOz pyrite raw B.C. and Utah Trail, B.C. 17 300 am ph Utah’ SO, smclter gls’ Esso Chemical Canada Redwater, 370 000 am ph Florida Sulphur Alta. Sherrin Gordon Mines Fort 50 000 am ph Florida Sulphur Limited Saskatchcwan, Alta. Western Co-operative Cakaary, 140 000 am ph Idaho Sulphur Fertilizers Limited Alta. Florida 724 000 Canada: installed capacity: mid 1986 964 000 historical capacity: end of 1983 I031 000 end of 1984 913000 end of 1985 788 000 end of 1986 698 000 P20s equivalent - Phosphorus pentoxide equivalent; am ph Ammonium phosphates. ’ Shutdown as ofthc end of June 1986. Shutdown in 1987. Phosphate now imported from Montana.

the beginning of this study in 1986,Cominco stillretained a entated towards niobium and rare-earth metals it did l~cate few phosphate leases north of Fernie,and in the Crowsnest significant phosphate potential on the Aley property. Pass and Line Creekareas. In late 1988 and early 1989 there In this study, which began in 1986, all available data has been renewed staking activity for phosphate, specifi- were collected and compiled in a province wide inventory cally in the Cabin Creek area and along Alexander Creek with the objective of identifying potentially economic de- north of the Crow deposit. In northeastern British Columbia posits. The compilation stage preceeded fieldworkin south- exploration has concentrated on phosphate of Triassic age eastern (1986) and northeastern (1987) British Columbia and recently on exploration for carbonatitedepositli. Explo- (Figure 5). This report summarizes the results of a twcs year ration workin conjunction with regional mappingprograms program. Interim reports have been publishedprevioudy in and stratigraphic studies by the Geological Survey of Can- the 1986 and 1987 editions of Geological Fieldwork and as ada has delineated the stratigraphic setting of phosphate ho- an open file (Butrenchuk 1987a,b; 1988). rizons and identified several significant phosphate During the compilation stage favourable stratigraphic occurrences. Although the carbonatite exploration was ori- horizons were identified and known phosphate occurrsnces

___ 4 Geological Survey E‘ranch ~~

Minisfry of Employment andI,w~l

to identify possible beneficiation problems and potential byproducts. A cursory evaluation of the subsurface phos- phatepoteutial wasalsocompleted. This portionofhestudy concentrated on an area paralleling the outcrop 0I’Triassic sedimentary rocks eastward to the Alberta border south of the Peace River. Northerly fromthe PeaceRiver the eastern limit was delineated bythe Alaska Highway. In addition to investigating bedded phosphate deposits the resource potential of carbonatites was also eraluated. The Aley deposit north of MacKenzie and the Vcrity CZ- bonatite north of Blue River were the only carbonatites in- vestigated. Other aspects of this study involved the sampling of tailings from the former producing Grauduc MineFor phosphate and titanium andthe investigation of FaleozJic strata in the Wells area eastof Quesnel where phosphate and base metal mineralization has been reported (A.B. Mawer, oral communication, 1987). Samples from this 1oca:ity were analyzed for phosphate, vanadium, barium., uranium, yttrium, lanthanum, cerium, copper and zinc. ACKNOWLEDGMENTS Figure 5. Lncation of study area Funding for this program was provided by the Can- were recorded for follow-up field examination. Fieldwork ada/British Columbia Mineral Development A;:reement consisted of an evaluation of reported occurrences and ex- (1985-1990).TheauthorgratefullyacknowledgesCominco Ltd., Crows Nest Resources Ltd., and Esso Minerais Canada amination of stratigraphic horizons known to contain phosphate. Phosphate localities were routinely sampled and, for providing pertinent phosphate data. Special gratitude is expressed lo A. Legun who provided analytical and pet- where possible, stratigraphic sections were measured. Sam- rographic data from his 1985 fieldwork in the Wpiti Lake ples were analyzed for phosphate using both x-ray fluore- area; to David Grieve for his logistical support throughout sence and wet chemical, volumetric techniques and for the 1986 field season and to Shaun Pattenden and David uranium, vanadium, yttrium, lanthanum, cerium and zinc Carmichael who provided ableassistance in the FLeld. Z.D. using x-ray fluoresence only.In addition, samples collected Hora is thanked for giving the author the opportu-lity to do from phosphate occurrencesin southeastern British Colum- this study andfor providing manyuseful suggesticns during bia were analyzedfor copper, lead, and arsenic. Specimens its course. Drafting of the final figures was done by J. Ar- were also collected for petrogrpahic and x-ray diffraction mitage and input of the manuscript was done by D. Bu- studies and whole-rock andtrace element analyses. Analy- trenchuk. The manuscript was critically reviewed by J. ses were done by the Analytical Laboratory of the British Newell who provided many useful improvemelts. Janet Columbia Ministry of Energy, Mines and Petroleum Re- Holland and Doreen Fehrare acknowledged for the exten- sources inVictoria and by Bondar-Clegg Company Limited sive and tedious work required to prepare this m:iterial for in Vancouver. Analytical and petrographic data were used printing and I thank themfor their many hoursof bard labor.

Bullefin 98 5

Ministry of Employment ond hrveslment

CHAPTER 2 PHOSPHATEDEPOSITS OF THE NQRTH AMERICAN CORDILLEXA

Extensive bedded sedimentary phosphate deposits occur along the western margin of the craton in the North American Cordillera (Figure 6). The best studied of these deposits are those of the Permian Phosphoria Fcnnation. The Phosphoria Formation covers an area of approximately 340 000 square kilometres and underlies parts of Iviontana, Idaho,Utah, Wyoming andNevada. Phosphatedeposits also occur at the base of the Mississippian in the Brazer limestone and Deseret limestone. The Phosphoria For.nation is the source of much of the phosphate rock impcrted into western Canada. In Alaska phosphate occurs extensively along the northern slope of the Brooks Range in the Mississippian Lisburne Group and the Triassic Shublik Formatisn. Their resourcepotentialisestimatedtobetensofbillionsoftonnes at greater than 10%Pzo5 (Patton and Matzko, 1959). Phos- phate deposits are associated with limestone, shale and chert. In the MacKenzie Mountains, immediately east of the Yukon - Northwest Territories boundary, phosphate occurs associated with calcareous shales and argillaceous limestones in the UpperOrdovician to Lower SilurianWhittaker Formation. A phosphatic chert, in strata possiblyequivalent in age,is associated with the Howards Pass lead-zincdeposit (Goodfellow and Jonasson, 1983). Throughout geological time there have bee.? distinct stratigraphic intervals in which phosphate deposition was more prevalent.Cretaceous and younger strata COT tain most of the world's phosphate reserves. The Permian WL:S another important period of phosphate deposition. Most of the Per- mian reserves are contained inthe Phosphoria Formation of the northwestern United States. In British Columbia phosphate occurs in formations that range in age .from Cambrian to Jurassic. These correlate well with phospho$.enic epi- sodes worldwide. Although none of British Coluclbia's extensive marine sedimentary deposits are presently economic, significant deposits are present in the Permian Ishbel Group andits equivalents in the Middle Triassic Sul- phur Mountain and Toad formations and in the Iawer Ju- rassic Fernie Formation. These deposits, \rhich are __" Figure6. Distributionof phosphatedeposits in theNorth American Cordillera: I-Baja,California:Miocene-Monten-eyanllSanIsidro Fms.: 2 - Montana, Idaho, Wyoming and Nevada:Pcrn ian - Pbos- phoria F~I.;3 - Southcastern British Columbia: Misrissippian - Exshaw Fm.; Pcrrnian - Ishbel Group and Jurassic- Femie Fm.; 4 - Northeastern British Columbia: Triassic- Sulphur Mountain and ToadFms.:5-YukonandNorlhwestTerritories(Mackc-lzieMoun- tains): Silurian Whiltakcrfin.: 6 -Alaska(Brooks Ranf:e): Missis- sippian - Lisburnc Group and Triassic- Shublik Fm.

Bulletin 98 7 British Columbia __ continuous throughout the Rocky Mountains of British Co- welling currents there is a proliferation of plankton and lumbia and parts of western Alberta, are described in detail other organisms that utilize phosphorus in their life ['roc- in the following chapter. Minor phosphate occurrences are esses. These biota settle tothe sea floor where some phos- present in Cambro-Ordovician, Devonian and Mississip- phorus is dissolved and returns to the sea and the remainder pian strata. is concentrated interstitially in the sediments. Phosphatc de- Carbonatites and related alkaline intrusions are the sec- posits can then form. ond most important source of phosphate worldwide. In Brit- Phosphate deposits can form by primary precipitation ish Columbia phosphate bearing carbonatites, most notably at theseawaterinterface, bydepositionofphosphatebezring the Aley and Verity intrusions, are known at a number of organisms or by diagenetic precipitation in ocean floor !:edi- localities. In addition to phosphate these carbouatites repre- ments (Sheldon, 1981). One or all of these processes may sent potential sources of niobium, tantalum and rare-earth be active atany given locality. elements (F'ell, 1987; Aaquist, 1981). The type of phosphate deposit that may form is depmd- ent upon the environment of deposition. Platformal phos- FORMATION OF PHOSPHATE DEPOSITS phate deposits are nodular in habit and veryoften associated with glauconite. Miogeosynclinal deposits are bedded, most How sedimenmy depositsdevelop has been the subject often pelletal and generally associated with black sh.iles, of much research and discussion over the years. Kazakov chert, and occasionally limestone. (1937) first postulated that they formed by direct chemical In British Columbia the majority of nodular depxits precipitation due to supersaturation when cold water en- are interpreted to have formed diagenetically. Most OF the riched in phosphorus rises and meets wanner upper waters nodules contain nucleii of varying descriptions, commmly that are more alkaline and contain less dissolved carbon di- one or more quartz grains, ammonite shells or other biodas- oxide. He concluded that deposition took place in the pho- tic material. Rapson-McGugan (1970) observed that com- tosynthesis zone at depths between 50 and 200 metres. paction of the sediment surrounding the nodule took place Kazakov observed that many of the phosphorites also as the nodule grew and displaced the sediment. Studies by formed in the border zone between shallow-water platform Burnett et al. (1982) of nodules of Holocene to Late Pleis- sediments and deep water geosynclinal basins. Although tocene age along the Peru-Chile continental margin show Kazakov's theory of upwelling is still accepted, other fac- that phosphate nodules grow slowly, at rates of less than 1 tors appear to be important in the deposition and corrcentra- to 10 millimetres per 1000 years. They observed that these tion of phosphate. His theory did not account for the suppression of calcium carbonate which normally precipi- nodulesoccuratthesediment-waterinterfaceandEormIlref- erentially near the upper and lowerboundaries of the oxygen tates under similar conditionsto those favouring phosphate minimum zone where it intersects the continental ma~gin. precipitation. In areas where there is high organic activity, They also noted that the nodules grow downward intc the it is possible for calcium carbanate tosuppressed be phos- as sediment. Deposition during the time of formation of these phate ion activity is increased. nodules is not necessarily slow. The source of the phospho- Specific conditions are essential for the formation of IUS and other elements contained in the nodules is believed phosphate deposits. An adequate source of phosphate is re- to be sedimentary interstitial water. Christie (1978) slates quired as are areaswhere phosphorus can be accunmlated. that the phosphate content of interstitial waters of marine Some form of trap is required. Upwelling waters and the sediments can be ten toa hundred times greater than th,atof right chemical conditions for apatiteprecipitation are also sea water. Phosphate rich water will phosphatize day, needed (Sheldon, 1981). A sedimentation rate which is very oozes, calcareous sediments and biogenic debris to form slow or inhibited is also important. The formation of rich fluorapatite just below the sediment surface. phosphatedeposits iscloselyassociated withrestrictedsedi- For some of the pelletal phosphorites it appearsthat the mentation and a high degree of stability in the basin and its pellets formed by the precipitation of phosphate from sea- supply of organic matter (Slansky, 1986). He postulates that water. In some of the Fernie phosphorites moulding 01' the it requires200 OOO to 1 OM) OOO years for a phosphate bed pellets around others suggests that they were probably de- 1 metre thick to be deposited. Some authors have related posited in a gel-like state at or below the waterlsedirlent phosphate deposition to diastemic conditions. interface. A few of these pellets also have quartz or carbon- The best areas for phosphate deposition are basin mar- ate nucleii. Elsewhere, especially in pelletal varieties of Tri- gins or near shoal areas. This is most evident in the Phos- assic age, there are textures suggesting that phospnate phoria Formation where the best deposits OCCUK at the formed as a replacement of calcium carbonate. The orig,inal structural hinge line between the stable shelf and the Cor- sediment is thought to have been a limestone or calcarcous dilleran miogeosyncline. Once the phosphate has been de- siltstone that has been wholly or in part replaced by phos- posited some reworking is required to concentrate it to phate. economic grades. One process of upgrading is the winnow- Most phosphate deposits appear to have formed within ing out of organic matter, clays and fine clasticparticles. 30" of the equator (Christie, 1980). Many ofBritish Colum- An adequate source of phosphorus is available in most bia's phosphate deposits do not meet this criterium. Paleo- seawater. It is estimated that the total phosphorus entering geographic reconstruction indicates that the Whktler oceans from all sources is 1.6 million tonnes per year. The member wasdeposited within 30" of the paleoeqnator (Irv- key factor is a concentrating mechanism. In areas of up- ing, 1979; MacDonald, 1985) while Triassic strata north of

~~ - ~~ 8 Geological Survey Bnmch Ministy of Employment and lrvestnrenf

Lemoray were deposited further to the north. Theoretically 1. Deposits in the phosphorite fields could represent poten- these more northerly exposures should not be expected to tially economical deposits; deposits plotting near the cac- contain extensive phosphorite deposits. However, although bonate or muscovite-clay end members may be difficult to not abundant, phosphorite has developed in more temperate beneficiate. climates as in the Jurassic FernieFormation. There areex- Figures 8, 9, 10 and 11 are diagrammatic repre- tensive nodular phosphate beds in the Toad Formation and sentationsfor phosphorites from the Permian, Toad and Snl- occasional thin phosphorite beds north of the ‘Tetsa River, phur Mountain Formations and the Fernie Fcrmation all of which are interpreted tohave formed in a temperate respectively.Anumberofs~mplesfromthePl~osphoriaFor- climate. mation are included for comparison. Many phosphate deposits in British Columbia are spa- Most of the phosphate-bearing rocks in tlie Permian are tially related to transgressive unconformities. MacDonald classified as phosphatic sandstones or siltstones (Figure 8). (1985) suggests that deep ocean circulation is speeded up Samples from Weigert Creek (57) are calcareous. Also, during periods of transgression or regression. This increased samples from both WeigertCreek and Nordstlum Creek can circulation should then be ableto supply more phosphate to be classified as the only true phosphorites. They arc slightly areas where all other factors required for the formation of more siliceous than phosphorite from the Phosphoria For- phosphate are favourable. The best deposits are those lo- mation. cated immediately above unconformities, an example of Samples from the Toad Formation (Figure 9) can be which is the phosphorite at the base of the Fernie Formation. classified as siliceous while samples from the ’Whistler member ofthe SulphurMountaiu Formation (Figur: 10) are CLASSIFICATION OF SEDIMENTARY distinctly calcareous and plot towards the carbonate end PHOSPHATE DEPOSITS member. For the Fernie Formation (Figure 11) there is a wide Phosphate rock occurs in a variety of forms many of variation in phosphate deposits ranging from very siliceous which are present in the British Columbia Cordillera. Vari- to calcareous. Western localities (Liz, 6 and 11) are carbon- ations in petrology are a reflection of the genesis of the de- ate rich whereas eastern localities are quartz rich. Tx Crow posits. Oolitic varieties aregenerally associated with a near deposit (4) is the only exception as it contains some carbon- shore, moderately agitated environment whereas structure- ate. A sample from Fording River (6) plots in theph’xphatic less pellets are formed in deeper water. Petrological vari- limestone-siltstone field corresponding to what is cbserved ations are also an important factor with respect to the in the field. beneficiation of phosphate rock. Phosphate deposits can also be classifiedaccording to Slansky (1986) proposed a classification of phosphate their iron and organic matter content (Figure 12). ‘The ma- rocks based on their physical characteristics, using the pa- jority of British Columbia phosphates are slightly to mod- rameters of grain size of the main phosphate fraction and erately carbonaceous or bituminous and generally the nature of the non-phosphatic fraction. This is mainly a non-ferruginous. A single sample from the Permiall (84) is qualitative classification. both highlycarbonaceous and slightly ferruginous. Interest- Mabie andHess (1964) while studying the Phosphoria ingly this sample is also anomalous in gold. Formation developed a more rigorous classification primarily orientated towards pelletal phosphorites. Their classifi- WEATHERING OF PHOSPHATE cation used a three component system consisting of fluorapatite or cdlophane, quartz and chert and muscovite- DEPOSITS sericite-clay as the three endmembers. The terms “calcare- Weathering is an important consideration.in thv$ evalu- ous” and “ferruginous” were used to describe phosphate taion of both sedimentary and carbonatite phosphatf:depos- mkcontaining more than 10% carbonate and 1 to 2% iron its as it may cause enrichment in the phosphate by 1:aching respectively. of the more soluble constituents. In some localitie?. within A more comprehensive classification is proposed for the Phosphoria Formation the Pz05 content may decrease British Columbia phosphate deposits based on Pettijohn’s byasmuchas5%belowtheoutcropsurface(Chene), 1957). A deposit mineable at surfacemay not beeconomic 2 t depth. (1957) tetrahedral classification of sedimentary rocks while retaining the compositional parameters established by Several factors affect the degree to which phosphate Mabie and Hess. A complete classification using the end- deposits areweathered. Weathering is more intense close to members phosphate, quartz, carbonate and muscovite and old erosion surfaces or faults that facilitate tlie movement clay is given in Figure 7. This classification is more quanti- of groundwater and hence weathering. Weathemi phos- tative while still retaining some petrological aspects of these phate rocks generally have a very lowcarbonate and organic deposits. It can be used to compare phosphorite deposits content. throughout North America. For deposits in British Colum- The effectsof weathering appear to be most plevalent bia this classification can he simplified to a three component in the Fernie Basin. Here, differential weathering has been system by using either carbonate or muscovite-sericite-clay superimposed on carbonate rich strata along its western as the third end member. The derivation of mineralogical margin and weakly calcareous shales alongits eastern mar- components in the Mabie and Hess classification and the gin. Alongthe western margin calcite dominates the gangue classification proposed in this study is detailed in Appendix mineralogy while along the eastern and southeasten mar-

.- Bulletin 98 9 P

Figure 7. Proposed classification for phosphate depositsin British Columbia.

(Numbers refer to those in Aqppendicer 3 and 13)

Figure 8. Cornpositional classification of phosphate-hearing Figure 9. Compositional classification of phosphate-bearirg strata of the Permian (after Mabie andHess, 1964). strata for the Toad Formation (after Mabie andHess, 1964).

10 Geological Survey Brmch Ministry of Employment and Lzvestment

Figure 12. Classificationof phosphatedepositsaccordiug to their organic and iron content (after Mabie and Hess, 1964),

gins of the Femie Basin quartz is dominant. and :alcite is only a minor constituent, locally becoming virtually absent. Dolomite is rare or absent throughoutthe Femie B.sin. The presence of yellow-orange weathering beds above :he phos-

~~ phorite is another indication of weathering. In the. westem Figure 10. Compositional classification of the Whistler member United States strongly weathered phosphatic strah contain phosphatebased on the three-component system: fluorapatite- a thin residuum of pale ordark yellowish orange mudstone quartzcarbonate. (Cheney, 1957). Similar beds were only observed in more easterly exposures ofthe Femie phosphate. These same exposures very often have a basal phosphatic conglomerate that is interpreted to have formed on an erosion surface. Thrust faulting is also much in evidence. Both of these features would promote weathering ofthe phosphate deposits. Weathering of surface phosphate has heen cited as the reason for differences in grade between surface md drill- core samples inthe Line Creek (Hannah, 1980) and Barnes Lake areas (Dales, 1978). The presence of blebsof limonite replacing pyrite grains indicates that some weahring has taken place. It is most pronounced in the Barnes Lake area and at the Lodge phosphate occurrence.In thin seclion there is noindication that Weathering has affected the phosphate pellets. Only minor weathering appean to have oa:urred in phosphorite of the Whistler member ofthe Sulphur Moun- tain Formation. Carbonateis abundant in the most :ioutherly exposures becoming rare at the northernmost locdity. Lo- cally many of the pellets have a lighter coloured rim suggesting that some organic matter may have been removed. The degree to which weathering has affected the phosphorite appears to increase northwards. Permian phosphatedeposits inBritishColumbiaappear have been less affected by weathering processel. Only surface exposures were sampled this in sudy and Figure 11. Compositional classification of the basal Femie phos- the depthto which the phosphate may have been w:athered, phate based on the three-componcnt system: fluorapatite-quartz- or how much the grade may have been affected were not carbonate. determined.

Bullerin 98 I1 ___ 12 Geological Survey Branch CHAPTER 3 STRATIGRAPHY OF SEDIMENTARY PHOSPHATE DEPOSITS IN BRITISH COLUMIBIA

REGIONAL STRATIGRAPHY is a disconformity of short duration between the Vega- Phroso and Whistler members of the SulphurMountain For- Bedded phosphate deposits in British Columbia occur mation. Phosphorite approaching economic grade occurs in a sequence of Helikian to Lower Jurassic marine strata above this disconformity. (Tables 2 and 3) deposited in a miogeosyncline along the western edge of the stable craton (Douglas and Price, 1972). Early Triassic deposition took place in a sta'11e shelf Depositional environments varied from platformal to basi- environment. The eastern limits of the shelf are marked by nal with phosphate occuning most often in platformal or bar and deltaic deposits (McCrossan and Glaistcr, 1964, shelf-edge facies. Douglas etal., 1970). During theMiddleTriassic deposition Cambrian to Mississippian strata consist of shallow- took place under partially restricted stagnant co~ditions. water carbonate assemblages that pass westwardinto deeper Lower and Middle Triassic sedimentsare charactc rizedby their uniformity and widespread continuity of stmigraphic water, more basinal limestone, shale and siltstone facies (Cecile and Norford, 1979; McMechan, 1987). During the units. Cambrian there were a number of marine transgressions Following the Late Triassic regression sediments of the with each successive transgression progressing further east- Whitehorse Formation (northeast British Columbia) and ward (McCrossan and Glister, 1964). Deposition of fine Charlie Lake Formation (Pine Pass area) wexe deposited in clastic sediments predominated through Ordovician and Si- a more restricted shallow-marine, intertidal and/or lagoonal lurian time. The Devonian is characterized by the develop- environment with an arid to semi-arid climate (DlJuglas et ment of widespread evaporitic conditions and the deposition al., 1970; Gibson, 1974.1975). At the same timesediments of platform carbonates. Phosphate deposition was restricted of the Lndington Formation were deposited in slightly to the Upper Cambrian and Lower Ordovician in north- deeper water in anenvironment that probably represents the eastern British Columbia. In southeastern British Columbia western margin of a tidal flat or intertidal shelf [Gibson, deposition of the first phosphate took place in the Upper 1975). A major unconformity marks the end of the Triassic. Devonian to Lower Mississippian Exshaw Formation. The remainder of the Mississippian is represented by crinoidal Another marinetransgression occurred in the Early Ju- limestone, argillaceous and cherty limestone and shale of rassic. Widespread deposition of phospholite and phos- the Rundle Group. These rocks were deposited in a shallow phatic shales began in Sinemnrian time with phosphatic shelf environment. shales persisting into the Toarcian. Sedimentation gradually became nonmarine at the end of the Jurassic in soul heastern During the Pennsylvanian, deposition of shallow-ma- British Columbia but marine deposition continued into the rine fine clastic and carbonatestrata took place under qui- Cretaceous in the northeastern comer of the provirse. escent conditions (Douglas et ai., 1970). Quartzitic sandstone and chert-bearing dolomite and limestone were The Rocky Mountains in which these beddcd phos- deposited in a neritic to littoral environment. phate deposits and marine strata occur are charactf.rizedby An unconformity marks the transition from Pennsylva- thrust faults and concentric folds. Thrust faults are i:enerally nian to Permian deposition. The Permian wascharacterized southwest dipping, concave upward and imbricat,:; north- by low hinterland relief and low-energy, shoreline condi- eastward displacements of up to 165 kilometres a1.e envis- lions (MacRae and McGugan, 1977) in which line-grained aged in southeastern British Columbia (Benver.uto and sandstone, siltstone, chert and minor shale and phosphate Price, 1979; MacDonald, 1985). Notable examples of these were deposited. Numerous marine transgressions and re- faults are the Lewis thrust with a displacement of 72 kilo- gressions resulted in a number of unconformities. In the metres (Christie and Kenny, in preparation), the Hosmer waning stages of the Permian, sabkha conditions appear to thrust west ofFernie and the Bourgeau thrust along the west have been present locally, resulting in the deposition of eva- side of the ElkRiver. While closely spaced thrust fs ults pre- porites. Phosphate deposition occurred at several strati- dominate in the southern Rocky Mountains, widel,! spaced graphic intervals and is frequently associated with the thrusts and more numerous concentric folds prevd in the unconformities. north. Mesozoic strata consisting dominantly of fine clastic A second important structural feature in the southeast sediments, unconformably overlie the Paleozoic sequence. is the Femie synclinorium. This double-plunging !.ynclinal During the Early Triassic there was a rapid marine trans- fold, which is outlined by the outcrop of the lurassc Fernie gression. Deposition was continuous through the early and Formation, has been the focus of phosphate exploration for middle Triassic except in the Wapiti Lake area where there many years. Several west-side-down normal faults cut

~" Bulletin 98 13 British Columbia -

TABLE 2 STRATIGRAPHY OF PHOSPHATE-BEARING FORMATIONS IN SOUTHEASTERNBRITISH COLUMBIA

Age Lithology Phosphate

Kmtenay Fm.

1-2 11-29

vvyyy VYVVVVI

" - nonphosphatic in Southeastern BritishCdumbia

wy regionalunconformity w_ vvvw YYVVUV\

Rangercanyon - smuence of chert. sandstone 0.6 9.5 Fm. (160) and siiklme: min&dolomite and gypsum: mngiomerats at base - shallw marine deposition - baa1 congtomeratezhertwim 0.5-1.0 13-18 phosphate pebbles pre~eni(61 metre)

" - phosphate in anumber 01 horizons as nodules and rneiy 0.4-1.0 1.7-6.0 dirreminatedgmules wimin me rnabix

wwc IvII\MIIp

0.3 I1.4

__I

1-22 0.1-11.0 0.2~0.3 3.0~4.0

1-2 14.2-21.2

lvvvu regibna1 ""conformity vvvu wwv VvvvYyI - dolomile silty, mmmonly 1.0 lr-1.3 contains chert nodules or beds

" Tunnel Mountain - dolomitiorandstoneand silktone Fm. (SM)

" MiSSiSSiPPiS., - limestone, dolomite, minorshale. sandstoneandchew limestone

- ~ Mississippiar - shale, dolomite, limestone

" 0.1 IS

1 610

0.1-0.3 1-9

" Pailiser Fm - limeslone "

14 Geological Survey Branch Minisrry of Employment and hvestment

TABLE 3 STRATIGRAPHY OF PHOSPHATE-BEARING FORMTIONS

IN NORTHEASTERN BRITISH COLUMBIA ~~~~ ~~ ,matan Lithoiqy Phosphate Thickness Grade hickness) (Meverl

I - Fernie Fm. -shale: sibtone. minor -a~pho~Phati~limest~ne 1- 250 - 9W limestone and sandstone: Of the Nomew member I ! l======RegionalUnconformityRiver(insh. Wapiti 1970) BaldonneiFm. dolomite."limeslone, Triassic (155) siltstone. sandslone: marine

siiktone. sandstone; marine Middleand Ludington Fm. - doiomiw to calcareous 400 siitslone. limestone: marine TriasiC

-1.5 netres Middle Triassic

", i pelletal phosphate nom of Richards Creek

1.24.6 0.31-l.! ,eves

minor phosphate in Regional Unconbrmity I==Permian "t Kindle Fm. I (701 I Flume Fm, (55-75)

" Kechika Fm. (15001

" lUpperCambrian -

Bulletin 98 15 though the centre of the synclinorium, including the Erick- phosphatic units are of interest only as marker horizorts or son and Flathead faults. as mineralogical curiosities. Another important feature throughout the Rocky Mountains is a general thinning of stratigraphic units east- CAMBRO-ORDOVICIAN PHOSPHATE ward. Thicker, more basinal deposits in the west give way to thinner shelf or platformal deposits in the east. UPPER CAMBRIAN An important factor in the evaluation of phosphate de- Investigation of Upper Cambrian strata was restri.:ted posits is the structural styleof the host rocks. In southeastern to the MountSheffield area in the headwaters of the Mus kwa British Columbia beds of Triassic or older age generally River at latitude 57'46' north, longitude 124"35' west (Fig- have gentle to moderate dips. TheJurassic Fernie Forma- ure 13). Lithologies consistof fine-grained sandstone,S.lale tion, being less competent, has absorbed much of the Struc- and siltstone. These rocks are thin to medium bedded and tural deformation and beds may have gentle tovertical dips. weakly calcareous. A grey calcareous siltstonethat contains In manyplaces beds of all ages are overturned and truncated lenses of phosphatic material outcrops at this locality by thmst faults. Elsewhere,especially in the Fernie Forma- (Cecile and Norford, 1979). Beds are 5 to 20 centimetres tion, thrusting has causeda repetition of beds, as atthe Crow thick and bedding planes are frequently marked by p)'rite property (Telfer, 1933). resulting in a thickening of the phos- bands 1 to 2 millimetres thick. The stratigraphic position of phate section. Areas where phosphate beds have beenthick- this unit may be in the uppermost section of the Upper Crm- ened by repetitive thrust faulting ofare particular economic brian sequence in strata equivalent to the Atan Group c,r in significance, as are areas of overturning where competent the lower part of the Kechika Formation. strata of the Triassic Sulphur Mountain Formation overlie Cecile and Norford describe the occurrence of phos- the basal phosphate and incompetent shale beds of the Ju- phate as black nodules in sporadic shale beds 120 to 220 rassic Fernie Formation. Imbricate thrust faults and over- metres below the bottom of the Kechika Formation. TLese turned folds are uncommon in Mesozoic rocks in the phosphate occurrences were notseen in outcrop during this northeast and are not an important consideration. To the study but similar material was found in talus. In addhion west inPaleozoic rocks the structure ismore complex where some thin, poorly developed pelletal phosphorite bed:; in locally thrust faulting is a signficaut structural feature. fine siltstonewere identified.

PHOSPHATE DEPOSITION KECHIKA FORMATION Investigation of the Kechika. Formation was restricted British Columbia phosphate deposits are of the miogeo- to a single locality in the vicinity of Grey Peak within synclinal type as defined by Christie (1978). The majority Kwadacha Provincial Park (Figure 13). Previous work by of the pelletal deposits arebelieved to have formed in a re- Cecile and Norford (1979) had documented the presenct: of ducing but non-toxic environment near the outer edgeof the phosphate at various intervals in the upper part of the for- continental shelf. Host lithologies are very often carbona- mation. This study focused on the uppermost unit of the ceous and the phosphorites are dark coloured as are the surrounding sediments. Pyrite often occurs in trace to minor amounts. Nodular phosphate deposits are interpreted to have formed in a platformal environment at or near wave base. In some of the Triassic deposits crossbedding is present in the adjacent rocks. Host rocks for Permian nodular phosphates are generally quartzose sandstones and siltstones. The Triassic Toad Formation nodular phosphates occur in carbonaceous shales, quartzose siltstones and fine sandstones. These sediments are locally calcareous and limestone beds are occasionally present. Phosphate deposition in British Columbia occurred principally in the Cambro-Ordovician Kechika Formation, the Devono Mississippian Exshaw Formation, the Permian Ishbel Group, the Triassic Toad Formation and Whistler member of the Sulphur Mountain Formation, and the Juras- sic Fernie Formation (Tables 2 and 3). There areminor occurrences in the Ordovician Road River Formation, the Devonian Flume Formation, the Mississippian Black Stuart Formation and the Late Pennsylvanian Kananaskis I''orma- tion. The Jurassic Femie Formation and thePermian Ishbel Group in southeastern British Columbia and the Sulphur Mountain Formation in the northeast contain phosphate de- Figure 13. Distribution of Kechika Formation and phosphab: posits of some economic significance while the remaining deposits in thc Grey Peak - Mount Sheffield area.

." ." 16 Geological Survey Brarich Minisfry of Employment and Iitvesfment

Kechika Formation (Unit OK4 of Cecile and Norford) and to the east, and in progressively deeper water to the west, lower units of the Road River Formation (Photo 1); the pres- towards Grey Peak.There isa corresponding westerly thick- ence of the phosphate beds was confirmed. ening of this formation towards tbe basin. Cecile and Norford divided the Kechika Formation into five units. The lower two units consist of platy and aren- ROAD RIVERFORMATION aceous limestones and aputty-grey weathering, nodular, ar- The Ordovician Road River Formation consist I primar- gillaceous limestone. A banded limestone overlies these ily of black siltstone and shale, calcareous shale and minor units and is overlain in turn by a thick sequence of argil- limestone. In the Grey Peak area (Figure 13 fine siltstone laceous, nodular calcilutite which is in excess of500 metres and graptolitic shale conformably overlie nodular Itmestone thick in the Grey Peak area. This nodular unit can be traced of the Kechika Formation. The lowermost unit is approxi- southward into the Mount Selwyn area (MacIntyre, 1981, mately 60 metres thick and very weakly phosphatic through- 1982; McMechan, 1987). Thin phosphate beds are present ont, containing very fine-grained phosphate clasts, in the upper 100 metres of this unit. The uppermost unit of sometimes associated with glauconite. The phosphatic unit the Kechika Formation consists of yellowish orange weath- is overlain by a non-phosphatic carbonate sequen(:e which ering limestones, not observed at Grey Peak. in turn is overlain by siltstone and shale. Phosphtie occurs Thin phosphate beds occur at fivehorizons in theupper in thin (1 centimetre) beds throughout the basal portion of 100 metres of the nodular limestone unit. Phosphate is pre- this upper clastic unit (Unit OR3 of Cecile and Norford, sent as microcrystalline coatings, 1 to10 millimetres thick, 1979). In 1989, a low grade phosphatic black shalt: was ob- around limestone nodules, and asphosphatized fossil debris served in Road River Formation in the area of Cassiar as- in beds 5 to 50 centimetres thick. Some pelletal and oolitic bestos mine (Hora and Nelson, personal communication, 1990). phosphate is also present. The phosphatic beds are recognized by their blue weathering surfaces and black colour The Road River Formation was deposited in i:shallow contrasting with the pale grey of the host limestone. Also basinal environment. The basal Road River records a period present, hut notobvious, are thin phosphatic coatings, 1 mil- of slow sedimentation as evidenced by the presence of phos- limetre or less in thickness, surrounding limestone nodules phate and glauconite. in beds two or more metres thick. Phosphate also occurs at several horizons in the lower banded limestone unit. Cecile DEVON-MISSISSIPPIAN PHOSPHATE and Norford describe these lower phosphate occurrences as “sea floor pavements or lag deposits”. EXSHAW FORMATION The Kechika Formation can be traced southeastward In southeastern British Columbia the earliest recorded through the Ware map area into the headwaters of the Ospika deposition of phosphate took place in the Upper Devonian River (MacIntyre, 1980) but no phosphate has been ob- to Lower Mississippian Exshaw Formation. This is a dis- served outside theGrey Peak area. tinctive, recessive black shale unit that forms an (excellent Cecile and Norford postulate that the Kechika Forma- marker. Exposures of Exshaw Formation are restricted to a tion was deposited in a shelf-margin environment. Deposi- narrow band inthe High RockRange, locally in the Flathead tion took place at the edge of a suhtidal carbonate platform River area, and in the Momssey Range south of Fernie. The

Photo 1. Section through Upper Kcchika Formation(K) and Lower Road River Formation (RR) near Grcy Pmk.

Bulletin 98 17 British Columbia best occurrences of phosphate occur north and south of A grab sample of typical material from this locality ,:on- Crowsnest Pass (MacDonald, 1985). tained 1.3% PzOs. Investigation of the Exshaw Formation was limited to a single outcrop on the south side of Highway 3, at the south- PERMIAN PHOSPHATE: THE ISHEEL west end of Crowsnest Lake. Here, the formation is in fault GROUP AND CORRELATIVE ROCKSI:V contact with the underlying Palliser Formation and is com- NORTHEASTERN BRITISH COLUMBIA prised of shale, fine siltstone, phosphatic shale and minor phosphate. A limestone hand present within the unit may Permian rocks extend throughoutthe Rocky h4ountains belong to the Banff Formation. The overlying shale may be of British Columbia. They unconformablyoverlie Pennsyl- a repetition of the Exshaw as there is a fault at the top ofthe vanian and Mississippian strata and are unconform:lbly limestone. Phosphate atthis locality is low grade (less than overlain by Triassic rocks. Regional correlations sire shown 4% PzOs) with the highest grade (3.60% PzOs) occurring in Figure 15. Phosphate deposits occur at several st:ati- above the central limestone band. graphic horizons within the Permian. Phosphate occurs at four horizons within the 13xshaw In southeastern British Columbia Permian strata are Formation (MacDonald, 1985). A basal phosphate, some- represented by the Ishbel Group which is comprised of.?our times present in sandstone overlying the top of the Palliser formations containing a number of phosphatic horizons. Formation, is absent at the locality on Highway 3. Three Phosphate is present in the Johnston Canyon, Ross Cmk other phosphate horizons occur in the middle and upper and Ranger Canyon formations. The Telford Formaticn is parts of the formation. non-phosphatic except for phosphate laminae and rardy, a very thin phosphate bed. In northeastern British Colnnibia The Exshaw Formation is conformably overlain by the the Permian is comprised of the Kindle, Belcourt, Fanto, Lower Mississippian Banff Formation,a sequence ofinter- Ranger Canyon, Fantasque and Mowitch formations bedded limestone, dolomite and shale 280 to 430 metres (McGugan and Rapson, 1964b) of whichthe latter two (:on- thick, in turn overlain by the Rundle Group, a resistant car- tain phosphate horizons. bonate unit also of Mississippian age, approximately 700 metres thick (see Table 2). Neither ofthese units are known The term Ishbel Group is not applied to strata in north- to bephosphatic. eastern British Columbia although stratigraphically equivalent rocks are present. The Kindle and Belcourt formations can hecorrelated with the upper part of the Johnston Canyon PENNSYLVANIAN PHOSPHATE Formation; the Fantasque Formation can becorrelated with the Ranger Canyon Formation. The Mowitch Formation is TUNNEL MOUNTAINFORMATION younger that the Ishbel Group. TheLowerPennsylvanianTunnelMountain Formation Phosphate deposits within the Ishbel Group have been of the southern Rocky Mountainsis described as a uniform, known since 1916 (de Schmid, 1917). These strata o(:cur monotonous sequenceofreddish brown weathering (lolomi- extensively throughout southeasternBritish Columbia (Fig- tic sandstone and siltstone (MacDonald, 1985). It isexposed ure 17, with their maximum development in the Tellord as far west as the Elk River (Figure 14, in pocket) where it thrust plate west of the Elk River and north of Spanv-Jod attains thicknesses in excess of 500 metres and thins east- (MacRae and McGugan,1977). The Ishbel Group has been ward to a thickness of 18 metres in the High Rock Range. correlated with the Phosphoria Formation of the wes'.ern Minor phosphate is associated with intraformational con- United States where extensive phosphate deposits are glomerate (1.22% PzOs across 10 centimetres) within this mined. formation in Alberta (MacDonald, 1985). The Phosphoria Formation whichis comprised of a sequence of shale, carbonate, chert, phosphorite and pltos- XANANASKIS FORMATION phatic shale is representative of miogeosynclinal deposits. The Middle Pennsylvanian Kananaskis Formation con- Facies variations indicate deposition in a basin that was formably overlies the Tunnel Mountain Formation. It con- deepest incentral Idaho and shallowerto the north, east and sists of a sequence oflight grey, silty dolomite and dolomitic west. It is estimated to have a resource potential of 22.5 siltstone. Chert nodules andintraformational chert breccias billion tonnes of which 1.5 billion tonnes are considered are found in the upper part of the section. This unit attains economic reserves. The phosphate content varies betwxn its greatest thickness (approximately70 metres) near Fernie 18 and 36%PzOs averaging approximately 25%.Phospk ate and gradually thins eastward. Its contact with the overlying is typically pelletal and consists of fluorapatite, quartz, mi- Permian Ishbel Group is unconformable and is generally normuscoviteandillite,andlesserorganicmaterial,carb3n- marked by a phosphatic chert-pebble conglomerate30 cen- ate and iron oxide. timetres thick. Locally, as in thevicinity of the Femieski- Permian phosphatedeposits in southeastern British 120- hill, this conglomerate bed is only 1 centimetre thick. lumbia and southwestern Alberta occur at several strati- Phosphate is rare in the Kananaskis Formation, re- graphic intervals. The Johnston Canyon and Ranger Canyon corded at only one locality adjacent to the MacDonald thrust formations are the most significant phosphate resource po- fault, where disseminated phosphategrains and rare nodules tential, because of their widespread distribution (MacDm- or intraclasts are present in a calcareous siltstone. Some ald, 1985,1987). Phosphateisalso present intheRoss Cr.:ek phosphate also replaces shell fragments or sponge spicules. Formation but its distribution is restricted and good expo-

." ." - 18 Gcological Suwyey Brunch AMERICAN SOUTHUST JASPER NORTHUSTCANADIAN RIVERMONTANAPEACE 'ON1RANGES B4NFF STANDARDTO B.C. B.C. NORTHWESTSUBSURFACE USA. SECTION WAPITI (BanffJasper) to 1 1

Forrlation?

~~~~~~ ~~~~ ~~~~ ,~~ ~~ ~ ~ Figure 15. Stratigraphic correlationof Pennsylvanian-Permian strata and phosphate horizons in the North American Cordi:lera (modified from McCrossan and Glaister, 1964; Bamber el al., 1968; MacDonald, 1985). sures are rare. Deposition was in a shallow shelf environ- few centimetres thick, marks the base of the fcrmation ment, with the eastern sequence being deposited close to a (MacRae and McGugan, 1977). Phosphate is prtsent as hinge line parallel to a shoreline trend (MacRae and black nodules in distinct horizons within sandstone, silt- McGugan, 1977). Host lithologies vary from conglomerate stone or calcareous siltstone beds at or near the base of the to fine-grained sandstone, siltstone and shale. Phosphatic formation. It is also present as phosphate-cemented :siltstone intervals vary considerably in thickness and grade. or as pelletal phosphorite. Phosphatic intervals range in Phosphate occurs in a number of forms but nodular va- thickness from less than 1 metre to a maximum of 2:1metres rieties are themost common. Phosohate nodules mav com- near MountBroadwood.

of Forsyth Creek. Pelletal varieties are relatively uncom- era1 pellets or of hioclastic debris. mon, but where present, grades are generally in excess of Pelletal phosphorite crops out north of Weigert Creek. 12%PZOS. PhosDbate Dellets 0.1 to 0.5 millimetre in size comorise 50 to 60% of the rock. The pellets are subroonded: ovoid, JOHNSTON CANYON FORMATION structureless and chestnut-brown to dark brown in colour, The Johnston canyonFormation, which unconfor- set in a matrix consisting mainly of quartz and calcite. mahly overlies Kananaskis or Tunnel Mountain strata, con- Phosphate, probably fluorapatite, cefnents quartz sists of a series of thin to medium-bedded siltstones and grainsin sedimentary rocks near the headwaters cf Not& sandstones with minor shale and chert. Locally these rocks strum Creek. Pelletal phosphorite is also present in a bed 1 are calcareous. A phosphatic chert-pebble conglomerate, a metre thick and containing 21.2% PzOs.

Bulletin 98 I9 ""

British Columbia

Photo 2. Phosphate laminae(blue-Black) in a sandstone bed, Telford Formation, Telford Creek.

Photo 3. Phosphatic coquinoid bed (blue) in Telford Formation, Telford Creek.

20 Geological Survey Brunch ~ ~ ~ ...... ~... . ~

Minisrry ofEmploymen1 and kvestment

TELFORD FORMATION These strata are postulated to have been depositell in two The Telford Formation comprises a thick sequence of environments: a shallow marineshelf starved of tenigenous material but able to produce clastic and authigenic phos- cliff-forming carbonates and sandy carbonates, generally phate; or a shoreline constructed of quartzose and phos- thick bedded andfossiliferous, that are preserved onlyin the phatic detritus. The depositional environment of the Ranger Telford thrust plate (MacRae and McGugan, 1977). Canyon Formation is compared to that of Baja, California, Phosphate is present in the middle part of thesection as where shelf phosphate, with associatedlag gravels, is form- a single nodularphosphatebed, 30 centimetres thick; a sand- ing offshore at the present time. stone bed containing fine phosphate laminae (Photo2); and The base of the Ranger Canyon Formation is marked a phosphatic coquinoid bed, 5 centimetres thick (Photo 3). by a phosphate-cemented chert-pebble conglomerate con- These occurrences were not documentedprior to this study. taining massive phosphate intraclasts (Photo 5). This con- Although thin, these beds appear to have been deposited glomerate was only seen beneaththe MacDondld thrust fault over a wide area under conditions of very quiescent sedi- in the Cabin Creek area. mentation. Phosphate also occurs in sandstone beds in the upper part of the formation where it ismost commonly presentas ROSS CREEKFORMATION nodules (Photo6) hut also as detrital apatite, amorphous and The Ross Creek Formation, preserved only in the Tel- crystallized fragments of bone material, pellets, rods, ford thrust plate, consists of a sequence of recessive, thin- spheres andoolites. Rapson-McGugan also noted that phos- bedded siltstone, argillaceoussiltstone, minorcarbonate and phate is the second most abundant clastic coinponlmt after chert (MacRae and McGugan, 1977). Nodular phosphate quartz, generally comprising 5 to 6% of the rock. Pkosphate occurs high in the section, associated with relatively thin is also present as phosphatic chert. Rapson-McGul:an sug- coquinoid beds (Photo4). The matrix in the coquinoid beds gests that much of thechert is a replacement ofpellelal phos- contains some phosphatic material. Pelletal phosphate is phorite resulting from solution of phosphate under acidic also present locally, as at the Elkford ski-hill. Unlike the conditions. If the solution becomes slightly alkaline, some other occurrences in the Ross Creek Formation, the phos- relict phosphate will remain in the chert. Cherts in the phate at thislocality occurs at the base of the formation, in Ranger Canyon Formation were not studied in detail. No an overturned sequence. petrographic or analytical work was done 011 therh in the course of this study. RANGER CANYON FORMATION Phosphate bedsin the upper part of the Ranger Canyon The Ranger Canyon Formation has beenstudied in de- Formation range in thickness from a few centimetres at tail and much of the information presented is summarized Mutz Creekto 4 metres at Fairy Creek, northof Fernie. With from Rapson-McGugan (1970) and MacRae and McGugan the exception ofa phosphate bed in thevicinity of th $ Fernie (1977). ski-hill, most are low grade. In southeastern British Columbia this formation, which Between Kakwa Lake and Wapiti Lakein northeastern unconformably overlies the Ross Creek Formation, is a British Columbia the Ranger Canyon Formation :onsists cliff-forming sequence ofchert, cherty sandstone, siltstone, predominantly of chert averaging 3 metres thick. It!; base is tine sandstone and conglomerate. Minor gypsum, as a pri- marked by a phosphatic, chert conglomerate. mary cement in sandstone, and dolomite are also present.

Photo 4. Phosphate nodules in a calcareous siltstone-coquinoid scquenceof the Ross Creek Formation north of Sulphur Creek.

Bulletin 98 21 Brirish Columbia ___

Photo 5. Basal conglomerate with phosphate cement(PC) and phosphate pebbles (P) in the Ranger Creek Formation, Cabin Creek area.

Photo 6. White-weathering phosphate nodulesin a siltstone from the Ranger Canyon Formation, Cabin Creekarea

22 Geological Survey Braizch BELCOURT FORMATION kon. It overlies younger Permian and Mississippian strata The Belcourt Formation is restricted to a narrow belt unconformably and is unconformably overlain by Triassic extending from Jarvis Creek north to Wapiti Lake (Figure rocks. Lithologies consistprimarily of chert with ninor in- 16) in northeastern British Columbia. It is approximately 30 terbedded siliceous mudstone and siltstone.The chmt is me- metres thick and consists of thick and thin-bedded silty dium todark grey in colour, locally pyritic, contain; sponge dolomite and limestone (McGugan and Rapson, 1964b). spicules and very often traces of phosphate. Chert nodules occur throughout the formation. The thick- Phosphate nodules occur in a siltstone bed at the top of ness of this unit is variable; no phosphate is known within the Fantasque Formation in the Burnt River area. 'The silt- it. It is assigned a Lower to Middle Permian age and may, stone bed is approximately 1 metre thick and conta ns10 to in part, be stratigraphicallyequivalent to the Johnston Can- 40% nodules by volume. It is believed to bestratigraphically yon Formation. equivalent to a siltstone bed in the Wapiti Lake area where two samples returned assays of 6.8 and 16.2% PzOsacross MOWITCH FORMATION thicknesses of 63 and 34 centimetres respectively (A. The Mowitch Formation is also restricted to a narrow Legun, personal communication, 1987). The auth.x intcr- belt in the front ranges of the Rocky Mountains between prets this horizon to becorrelative with a similar be3occur- Jarvis Creek and Lemoray in northeastern British Columbia ring at the top of the Ranger Canyon Formation near:Counor (Figures 16 and 17). It conformably overlies chert of the Lakes in southeastern British Columbia (Butnmchuk, Ranger Canyon Formation and consists of thin, brown, 1987). and to the bed at the top of the Mowitch Fdrmation phosphatic, siltstone to fine sandstone. The uppermost bed, at Meosin Mountain and Wapiti Lake. which is approximatley 1 metre thick, is characterized by the presence of black, ovoid phosphate nodules. This nodu- BELLOY FORMATION lar phosphate-bearing siltstone bed which is exposed at Subsurface strata in the Peace River district, ey:Jivalent Wapiti Lake and Meosin Mountain is similar to a nodular in age to the Fantasque and Ranger Canyon formations are unit seen in the Connor Lakes area, except that the nodules assigned to the BelloyFormation, consisting of a lokrcar- are smallerand more abundant. bonate member, a sand member and an upper carbonate member. Phosphate may be present in all three msmbers. The Mowitch Formation is unconformably overlain by shale and siltstone of theVega-Phroso member of the Trias- Phosphatic fish remains are present in the Sand meglber and sic SulphurMountain Formation. The depositional environ- glauconite is a major component of the sand. ment is considered to be shallow water in close proximity The upper carbonate member consists of )imy to to the eastern shoreline of the basin (McGugan andRapson, dolomitic, fine-grained quartzose sandstones that griide into 1964b). dolomitized limestones and bedded cherts (Halb,ertsma, 1959). Phosphatic fish remains are common and a phos- KINDLE FORMATION phate-rich horizon, varying from a few centimetres lo in ex- The Kindle Formation outcrops in abelt along the west- cess of 2 metres, is reported near the topof the formation (J. ern Rocky Mountains from the Halfway River northwards MacRae, oral communication, 1988). to theToad River, with the best exposures between the Rac- ing andToad rivers (Taylor and Stott,1973) (Fip,UIeS 18, in TRIASSIC PHOSPHATE pocket, to 20). Triassic strata in northeastern British Columbia are ex- This formation, comprising a sequence of siltstone, posed in a north-northwest trending belt from theAlberta - shale, siliceous limestone and chert, unconformably over- British Columbia boundary at 54" north latitude into the Yu- lies older strata and is unconformably overlain by the Fan- kon (Figure 21). This study focused on Lower and Middle tasque Formation. It is 90 to 205 metres thick with the Triassic strata in which phosphate has been reported lby Gib- variation in thickness being due to erosion prior to deposi- son (1971, 1972, 1975) and Pelletier (1961, 1963, 1964). tion of the overlying rocks. Phosphate-bearing strata are lo- The Sulphur Mountain Formation south of Pine Pass and the cally present near the top of this formation, in exposures Toad and Grayling formations north of Pine Passare of par- along the Alaska Highway immediately east of Summit ticular interest. Correlation ofthe various stratigraphic units Lake. The phosphate is present as black, wispy lenses and is shown in Figure 22. laminations in a dark grey siliceous shale associated with Triassicsedimentationtookplaceonastablesbelfchar- phosphatic chert. acterized by a pattern of embayments and platforms. Ami- At Mount Greene, north ofthe Peace River, phosphatic norembayment, flankedto the south by the Wapiti platform horizons were noted in strata underlying the Ranger Canyon and tothe north by the Nig Creek platform, develop4 south Formation (McGugan, 1967). These rocks are tentatively of Fort St. John during the Early Triassic (McCrossan and correlated with the Kindle Formation (Bamber el a[., 1968) Glaister, 1964) (Figure 23). These conditions prevailed into and are lithologically similar to the Johnston Canyon For- the early Middle Triassic and probably exerted some (control mation in southeastern British Columbia. on phosphate deposition. The majority of the known phosphate occunencs, and FANTASQUE FORMATION phosphatic sediments occur in the Whistler memhel. of the The Fantasyue Formation of Permian age outcrops in a Sulphur Mountain Formation and incorrelative rock:;of the semi-continuous band from north of Lemoray,into the Yu- Toad Formation (Figure 24) both of Anisian age. Phwphate Figure 16. Distribution of phosphate bearing strata in the Monkman Pass - Sukunka River area (931 and 93P).

~~~ ~~ ~~ "~~~ ~~ ~~ ~~

~ ~~ ~.~~ "" SUMMARY OF SUBSURFACE WELL DATA

Map Drillhole Latitude Longitude Phosphatic Comments No. Interval (metres)

1 Triad Prairie 54"36'08 lZO"32'37" 1112 - 1125 Trace phosphate pellets in a-24-H shale -Toad Fm.

3024 ~ 3030 Phosphate pellets in shale - Toad Fm.

2 Quasar Union Onion 120'36'36" 54'38'30"869 ~ 872 Phosphate pellets in sandstone- c-69-H Toad Fm. 984 - 987 Coarse phosphate pellets in shale -Toad Fm.

1000 ~ 1003 Phosphate pellets in shale Toad Fm.

~~ 24 Geological Survey Brar,ch 15' 30' 45' 1s 12.TO0' 56'0C '* F 513'00' I

KILOMETRES

45 413'

SECTION 70-31 -8 Phosphate nodule9 at base of Toad Fm.

. jS30 Sample numbers 5730' LEGEND SB87-16 to 21

s:Eie Formation TRIASSIC PardonnetFormation

~ SulphurMountain Formation

Graylingand Toad Formations (mayinclude younger 15' Triassicstrata) PERMIAN SECTION 71 -30- FantasqueFormation

=GeologicalSurvey of CanadaSection 71-30-2 (paper no. andsection no.)

Phosphatelocality described in text NUMBER LOCATION MlNFlLE NUMBER 33 Baker Creek 0930 038 34 1.emoroy 0930 011 5'00' , "_"" 1 5' 123'00' 45' 30' 45' 123'00' 15' 15' 122'00'

Figure 17. Phosphate depositsin the Mackenzie map area (930).

Bulletin 98 25 i3'30'

LATITUDE 5~29'1a" LONGITUDE 12510'50" PHOSPHATICINTERVAL (METRES) 1091-1094 COMMENTS: PHOSPHATEGRAiNS IN SHALE- MONTNEYFM (TOP AT 1112)

LEGEND

CRETACEOUS

FIGETHiNG FORMATION, andBuckinghorse Formation

TRIASSIC 8'15' XL 1 LIAR0FORMATION

TOADFORMATION

GRAYLINGFORMATiON

PERMiANAN0 MISSISSIPPIAN w[PROPHET FORMATION (includes Fontasque andKindle Formations)

x p2 0, PHOSPHATEOCCURRENCE

NTS 94J 12coo 12530' ___

Figure 19. Phosphate deposits in the southwest corner of the Fort Nelson map area (941). Figure 20. Geology and phosphate deposits in the Tetsa River area(941(/9), is present in a variety of forms including pelletal phos- VEGA-PHROSO MEMBER phorite, nodules, phosphate cement, phosphatic fragments The Vega-Phroso member of EarlyTriassic age uncon- or clasts and phosphatized fossil debris. Minor phosphateis formably overlies Permian strata. It is typically a flaggy, also present at a fewlocalities in the Vega-Phroso and Llama brownish weathering unit consisting of grey siltstone and members. calcareous siltstone with minor shale and bioclastic limestone. Thin phosphatic beds(10-20 cm) occurlocally in the SULPHUR MOUNTAINFORMATION upper part of the section. The unit varies from 81 to 272 metres in thickness. The Sulphur Mountain Formation unconformably overlies the Ishkl Group south of Pine Pass. It typically WHISTLER MEMBER consists of a rusty brown-weathering sequence of mediumbedded siltstones, calcareous and dolomitic siltstones, silty The Whistler member, whichoverlies the Vega-Phroso dolomite and limestone, and minor shale. It attains thick- member disconformably,is a recessive unit, 20 to 85 metres nesses of 100 to 496 metres, thickening northward, and was thick consisting of grey-weathering dark grey siltstone, deposited in a shallow-water, deltaic environment (Gibson, shale and limestone. It outcrops in a northwesterly bending 1974). It isnonphosphaticin southeasternBritishColumbia. belt that extends from Meosin Mountainin the southeast to Watson Peak in the northwest. This unit tendsto be darker InnortheasternBritishColumbiatheSulphurMountain in colour than boththe overlying and underlying members. Formation is subdivided into the Vega-Phroso, Whistler and At many localities its lower contact is marked by a phos- Llama members. The formation consists of shale, siltstone phorite bed that may contain a thin (5 to 20 cm) basal phos- and limestone and exhibits a general thickening westward. phatic conglomerate. This basal conglomerate was not seen Phosphate occunin the Whistler member (Heffernan, 1980; in sections measured at Meosin Mountain but is present in Jxgun and Elkins, 1986) extending fromthe British Colum- the Wapiti Lake area. Elsewhere phosphatic and phos- bia - Alberta boundary to northwest of the Sukunka River. phorite beds are present throughout Whistler memoer. At Further to the north phosphateis present inthe Toad Forma- Watson Peaksiliceous phosphate lenticles are reportc:d to be tion which is stratigrapbically correlated with the Sulphur presentintheupperpartoftheunit(Gibson,1972).Bs:tween Mountain Formation. Wapiti Lake and Mount Palsson phosphorite beds cmmtain-

Bulletin 98 27 British Columbia __

by detritus. There may also have been some winnowinl: of

LEGEND detrital material, to be more concentrating the phosphozite. Phosphate is interpreted to have been deposited in a shallow-water, high-energy environment above normal wave base (Gibson, 1975) during a marine transgression. Following the deposition of phosphate there was a deer ening of the seas and conditions returned to those of deposilion in a more basinal environment, below normal wave t'ase along the outer margin of the shelf. MacDonald (1985) en- visages that phosphate was deposited on an oxygenated intertidal or subtidal flat during a stillstand period at the end of the Lower Triassic. Phosphate was deposited envi~on- ment.

LLAMA MEMBER The Llama memberis a resistant sequence of dolomitic and quartzitic siltstone and limestone with minor sandslone and dolostone, conformably overlying the Whistler mm- her. It varies in thickness from 60 to 360 metres. Phosphate is reported in the lower part of this unit at a single section measured at Meosin Mountain (Gibson, 1972).

GRAYLING FORMATION The Grayling Formation comprises strata of Early Tri- assic age north of Pine Pass and is comelatable with the lower part of the Vega-Phroso member of the Sulphur Mountain Formation. It consists of recessive, flaggy argillaceous siltstone, dolomitic siltstoneand silty shale. Strata containing phosphate nodules are locally present in the upper part of the formation. The Grayling Formation, where present, unconformably overlies strata of Permian or Ivlis- sissippian age and is conformable with the overlying 'bad Formation.

TOAD FORMATION The Toad Formation comprises Early to Middle Trias- sic strata north of Pine Pass. It iscorrelatable with the upper Vega-Phroso, Whistler and lower Llama members. Ilpi- cally it consists of grey to dark grey weathering, generally darkgrey siltstone, shale,calcareoussiltstone andsilty limestone, most of which are weakly to moderately carbonaceous. It varies in thickness from 155 to 820 metres, wi h an average thickness in excess of 300 metres. Phosphate occurs in numerous beds throughou: the middle part of the formation. The phosphate-bearing interval varies in thickness from a few tens of metres to app :oxi- Figure 21. Distribution ofTriassic stratain nolthwestern British mately 290 metres. The basal part of the phosphatic section Columbia. generally contains calcareous, ovoid concretions seieral centimetres in diameter. Phosphate is present as nodules, ing phosphate grains and oolites occur at three distinct stra- phosphatic lenses, phosphate cement and occasionally as tigraphic horizons. Coarse to very coarse-grained phos- pellets and asphosphatized fossil debris. Phosphorite is rare, but where present, consists of pellets, few oolites and nod- phate, some of which is oolitic,is reported to be present in ules in a carbonate-quartz matrix. Many of the pellets have a section measured in the Wolverine-Suknnka River area an irregular carbonate core suggestingthat replacement of (Gibson, 1972). Gibson (1975) suggests that thebetterphos- carbonate by phosphate may have taken place. Also pr:sent phate Occurrences are associated with ''shelf' or thinning in the cores are quartz, feldspar, shell fragments and rarely trends reflecting areas of nondeposition or extremely slow pyrite. Pelletal phosphate is exposed at Richards Cree:< and sedimentation where phosphate deposition was not diluted along the Alaska Highway north of the Tetsa River. __ 28 Geological Survey Branch Figure 22. Correlation between Triassic formations and membersof surface and subsurface areasof British Columbia andAberta

~~ ~ ~ ~~ ~ ~~ ~ (modifiedGibson,from 1975). ~ ~~

Figure 23. Paleographic map of the Early Triassic (after McCrossan and Glaister,1964).

~ ~~~~ ~ ~ ~~~~~~~ ~ ~ ~~ ~~~ ~ ~~~~~ _" Bulletin 98 29 2 WHITEHORSE z Ministry $Employment and Investment

LEGEND 0Phorphate bearing s8qumce Sondrione Silirione

Shale

Limestone

CDnglomerale

Caicoreaus shale

Chert

Siltstone and dolomite

Dolomile

Figure 25. Stratigraphic position, thickness and colrelationof phosphate-hearing strata on surface and in the subsurface, Hall'way River - Trulch map sheets (94B and 94G). Deposition of the Toad Formation is interpreted to have tion occupies a broad canoe-shaped synclinal structure cov- taken place in a deeper water, less restricted, open marine ering an area of 2000 square kilometres and attains thi':k- environment. nesses of 70 and 376 metres with a general thicken.ng westward (Figure 14, in pocket). A persistent pelletal phos- WHITEHORSE FORMATION phorite bed, 1 to 2 metres thick and generally contahng In northeastern British Columbia the Whitehorse For- greater than 15% PzOs was deposited in a transgressive se- mationisrestrictedtotheSukunkaRiver-MeosinMountain quence at the base of the Femie Formation in strata of Si le- area where it overlies the Sulphur Mountain Formation murian age. It rests either directly on Triassic strata 01' is (Gibson, 1975) (Figure 16, in pocket). Deposition toolcplace separated from the underlying rocks by a thin phosphatic under very shallow water and probably evaporitic condi- conglomerate. The phosphatic interval may also be repre- tions, in a broad intertidal to tidal flat environment. Strata sented by two phosphate beds separated by phosphitic in this formation include dolostone, sandstone, siltstone, shale. Thicknesses in excess of 2 metres are attained locally, limestone and minor gypsum. as at Mount Lyne where 4 metres of phosphate rock are In southeastern British Columbia the Whitehorse For- present. Phosphatic shales of variable thickness, generzlly mation is poorly developed and is restricted to the areas west less than 3 metres, overlie the phosphate. The top of this of the Elk River north of Elkford; north of Grave Lake; and sequence is sometimes marked by a yellowish orange c al- in the Flathead River area south of Fernie (Gibson, 1969). careous bed 2 to 5 centimetres thick. Thin marcasite b(:ds It varies in thickness from 6to 418 metres and consists of may also be present locally within the phosphatic interval. an assemblage of pale-weathering, variegated dolomite, A second phosphate horizon lies approximately 60 ne- limestone, sandstone and intraformational breccias (Gib- tres above the base of the Fernie. It is low grade (less than son, 1974). Its contact with the underlying Sulphur Moun- 1% PzOs) and sometimes associated with a belemnite-bear- tain Formation is gradational and its contact with the ing calcareous sandstone horizon. This horizon was o~ly overlying Fernie Formation is disconformable. It is non- observed above the railroad tracks south of the Highwa,y 3 phosphatic. roadcut at Alexander Creek and ina poorly exposed outc~'op north of Mount Lyne, where it occurs in shale rather than TRIASSIC SUBSURFACE DEPOSITS sandstone. Evaluation of subsurface phosphate potential was restricted toa narrow belt paralleling the outcrop of Permian In northeastern British Columbia exposures of Fernie and Triassic sediments. In the subsurface, phosphate occurs Formation parallel Triassic strata from the Jarvis Creek area in the Middle Triassic at the contact between the Doig and to the Sikanni Chief River where the formation pinches ,out Montney formations or in rocks of equivalent age (Figure (Figures 19,20 and 21, in pocket). Exposures are restricted 25). to the foothills area. North as far as Wapiti River the basal Phosphate is present as pellets, grains or occasional sequence consists mainly of black phosphatic limestone. nodules. Pellet contentvaries from trace to 25% and rarely These strata, assigned to the Nordegg member, are of Six- as much as 80% . In a few wells phosphate is reported as murian age, and are equivalent to those in the FemieBasin bands, stringers or lenses comprising asmuch as 30%of the of southeastern British Columbia. In the Halfway Ri,m rock. Host lithologies aredark grey toblack shales and dark area, equivalent strata consist of recessive, fissile, dark gxy brown to grey siltstone. Limestone is occasionally present. to black, calcareous shale (Irish, 1970) with no repor!ed All of these rocks are weakly calcareous, occasionally phosphate occurrences. dolomitic and rarely glauconitic. Pyrite is reported, but also The Nordegg member of the Femie Formation was (le- it israre. A phosphatic conglomerate is reported in one hole posited in a shelf or platformal environment. Glauconitc is (Home eta[.,Minaker). Phosphate-bearing intervals usually commonly reported in the subsurface in the Peace Rim produce a high radioactive response on gamma-ray logs. area; chert is present in surface exposures. To the southwest In some of the wells siliceous or cherty black shale pel- theenvironment changes toabasinal facies.Sediments w,:re lets are reported in Triassic strata where phosphate should deposited in fairly deep water under reducing conditions. be expected. These may in fact be phosphate pellets that Pellets are believed to have formed authigenetically below have not been recognized. the water-sediment interface. The presence of pyrite sup- ports the reducing environment. Cross-stratification and JURASSIC PHOSPHATE other indicators of shallow-water deposition are not sesn, hutmoderatecurrentactivityisevidencedbyoccasionalrip- FERNIE FORMATION ple marks seen on the eastem margin of the Fernie Basin. Triassic strata are nnconformably overlain by dark grey Deposition along the western margin of the basin probably to black shales, phosphate and minor limestone, siltstone took place in a deeper water environment where poorer and sandstone of the Jurassic Fernie Formation (Freebold, phosphorites and mainly calcareous matrices were devel- 1957, 1969). In southeastern British Columbia this forma- oped.

32 Geological Survey Branch Ministry ofEmployment and Inwstment

CHAPTER 4 PETROGRAPHY AND MINERALOGY OF SEDIMENTARY PHOSPHATE IN BRITISH COLUPVII~IA

KECHIKA FORMATION phosphatic material is difficult to distinguish in thin section Phosphate in the Kechika Formation is present as thin because ofthe fineness of the sediment andits ~:arbonaceous content. Phosphate is probably present minute grains or phoscrete layers 1 to 10 millimetres thick, as pellets, and as as possibly as cement. phosphatized trilobite remains (Photo 7). The phoscrete consists of colour-banded microphosphorite laminae that EXSHAW FORMATION form a continuous surface except where broken bycalcite- filled microfractures. Thin layers have been broken and in- Thin sections show that the phosphate occurs as dispersed pellets 1 millimetre or less in size. They we suh- corporated into overlying beds. Pellets that are distinctly rounded and constitute approximately of the rock by oolitic occasionally have carbonatecores. Very often broken 10% pellets andphosphatizedshell debris are found togetherwith volume. Most ofthe pellets are structureless although a few broken phoscrete fragments in limestone overlying pre- are nucleated. MacDonald (1985) observed that most ofthe served phoscrete beds. phosphate isalso pelletal with nucleatedandoolitic varieties predominant. Structureless nodules and intraclasts are also The microphosphorite laminae canbe present as either present. The basal phosphate consists of nodules up to 2 distinct beds or as thin veneers surrounding limestone nod- centimetres across, bone fragments, intraclasts and nucle- ules. Carbonate and phosphategrains with concentriclayers ated and rimmed pellets; the uppermost phosphate horizon of microphosphorite are the most distinctive pellets present consists of a conglomeratic mixture of nodules, bonefrag- in these phosphatic horizons. ments and minor pellets and intraclasts (MacDonald, ROAD RIVER FORMATION 1985). The form in which phosphate is present in the Road ISHBEL GROUP River Formationis not readily apparent. There are thin black Phosphate, as fluorapatite, is present in thl: Ishbel phosphatic laminae in the lower part of the formation, but Group as nodules, pellets, cement, (Photo 8) intraclasts and

Photo I. Photomicrograph (40x) showing phosphatic oolitesand broken phoscrcte layers from the Kechika Formation, Grey Peak.

Bulletin 98 33 British Columbia -

as replacement ofbioclastic debris that includes brachiopod lar to subrounded and generally wellsorted. Feldspar, dith shells, sponge spicules and possibly foraminifera. varying amounts of calcite, is also present in the mauix. The nodular variety is most common, occurring Dolomite, albite and illite may be present in minor amounts. throughout the Permian section. Nodules are most prominent in the Johnston Canyon and Ranger Canyon forma- SULPHUR MOUNTAIN FORMATION tions, commonly occurring as ovoid structures thdt vary Phosphate is present in the Whistler memberof the S,'ul- from l centimetre to greater than 7 centimetres in diameter phur Mountain Formation predominantly as pellets $ith (Photo 10). Locally they have irregular shapes and may be lesser nodules, phosphate cement and phosphatic biocla:;tic elongate parallel to thebedding. Internally they may contain material. one or more quartz nuclei as well as bioclastic material The pelletal phosphorite occurring at the base of the (Photo 9). Composition ofthese nodules is given in Table4. unit has the mostsignificance (Photo 11). It iscomprised of Pelletal phosphorite was observed onlyin the Johnston brown, dark brownor black pellets with occasional nodules Canyon and Ross Creek formations. Pellets are generally and locally, phosphate cement. The pellets range in !;ize structureless (Photo IO) although oolitic pellets, and a few from 0.05 to 0.5 millimetre and are variably sorted. Fivw to others, have a radial structure. Less than 15% of the pellets fifty percent of the pellets are either nucleated os encased are nucleated or encased; quartz, and to a lesser degree cal- with approximately varying amounts of quartz andcalcite. cite, form the nuclei. Size of the pellets varies from 0.1 to Oolites comprise 1 to 15% of the pelletal material. %me 0.5 millimetre. These pelletal varieties have semidispersed phosphatized bioclastic debris is also present and is erpe- to dispersed textures. cially significant immediately south of Meosin Mount.Jn. Phosphate is present as cement throughout the Ishbel At this locality phosphate pellets are dispersed throughout Group. Primary cement was observedin the basal conglom- a bioclastic matrix that has been partially or wholly phos- erate of the Ranger Canyon Formation as well as in tine phatized (Photo 12). clastic rocks of the Johnston Canyon and Ross Creek for- The matrix in the phosphorite is dominantly calcite al- mations. Phosphatecement isusually a brown colour inthin though locally the matrix is quartz rich. Minorconstitumts section. include feldspar and dolomite, and locally, fluorite. Quali- Complete or partial replacement of bioclastic debris is tative abundances ofthe minerals present in Whistlermt:m- most prominent in the Ross Creek and Johnston Canyon ber phosphate rocks are given in Table 5 and the relative formations. Intraclasts are not abundant; where present they abundances ofthe major mineralsare given in Appendix20. contain quartz nuclei that differ in grain size from quartz in Grain size of the matrix is also variable, most often smrller the matrix or contain several phosphate pellets. than the pellets. Locally, where the matrix is almost totally carbonate, the grain size of the pellets and the matrix may Host lithologies in the Ishbel Group are quartz-rich silt- be the same. stones and fine-grained sandstones. The quartz is subangu-

Photo 8. Photomicrograph (40x) showing phosphate pellets (P)and phosphate cemcnt (PC)in a quartz-rich (Q)siltstone from the Johnston Canyon Formation, Mount Broadwood.

34 Geological Bnznch Survey Ministry of Employment and ihvestment

Photo 9. Photomicrograph (40x) of phosphate containing phosphatc pellets (dark brown), quartz grains (white) and shell material fromthe Ishhel Group, Crowsncst Pass area.

Photo 10. Photomicrograph (40x) of disseminated phosphate pellets (P)in a quartz (Q)-calcite (Cc) matrix in thebasal Johnston Canyon Formation from the Fenster Creek area.

Bulletin 98 35 British Columbia

TABLE 4 TABLE 5 QUALITATIVE MINERAL ABUNDANCES IN THE QUALITATIVE ABUNDANCE OF MINERALS IX PERMIAN PHOSPHATES THE WHISTLER MEMBER OF THE SULPHUE. (Determinedby x-ray diffraction) MOUNTAIN FORMATION

~ ~~~~~~~ ~~ ~~~ ~ ~~~~ (Determinedby x-ray diffraction)

SampleLocationMinerals Identified ". .. ~ ~~ NO. SampleLocationMinerals ldcntificd

SBB86-ZB MutzQuartz> fluorapatite> dolomite > Creek minor K-feldspar.minor Creek SB87-6 Meosin Calcite ?fluorapatite >> Ininor (.uartz, SBB86-61 LIadncr Fluorapatite quartz >> minor Mountain illite and dolomite. (noduics) Creek(noduics) dolomite, K-feldspar. SB87-7(4) Meosin Calcite >> quartz > fluorapatite strace SBB86-71 Crowsnest Fluorapatite > quartz. Mountain dolomite. (nodules) Pass SB87-11(2) Wapiti Fluorapatite > quartz > Calcite >> trace SBB86-79(2) Nordsrmm Fluorapatite > quartz >> minor Lake dolomite, feldspar and illite. (nodules) Creek(nodules) daiomitc, K-feldspar. SB87-IZ Wapiti Fluorapatite >> calcite > quartz >>trace SBB86-85(2) MacDonald Fluorapstitc? quartz>>calcite >> Lake dolomite. ThrustFault trace K-feldspar. SB87-15 Mount Fluorapatite > calcite > quartz > minor SB87-45 Alaska Calcite > quartz > dolomite > apatitc Palsson doiomitc > trace iilitc andfeldspir. Highway buddingtonite.Highway

Photo 11. Photomicrograph (40x)of pelletal (P) and oolitic (0)phosphate in a quartzosc matrix from the Whistler member of thcSulphur Mountain Formation, Wapiti Lake.

Many ofthe pellets exhibit textures suggestingreplace- bioclastic debris are also present. Phosphate cement is ]'are. ment of original carbonate, possibly an oolitic limestone, Much of the carbonaceous and calcareous siltstone in the that has been replaced or diagenetically altered to phos- middle Toad Formation is weakly to very weakly pnos- phate. Elsewhere alternating carbonate and phosphaticlay- phatic; phosphate is present as distinct detrital grains as ers in the oolites suggests that there may have been some shown in Photo 13. periodicity to the phosphate and carbonate availability Nodules occur as black, ovoid structures, 1 to 3 cmti- while these oolites were forming. metres in size. They occur in beds ranging from a fraction of a metre to in excess of2 metres thick, although beds over TOAD FORMATION 2 metres thick are rare. The nodules contain numerous small The dominant form of phosphatethe in Toad Formation nucleii, or a rarely, a small ammonoidand areinterpret€ d to is nodular, but pelletal phosphate occurs in more northerly have formeddiagenetically. Many appearto have forme3 by locations and phosphatized fish skeletons, ammonoids and replacement of carbonate, primarily calcite. Nodules with Photo 12. Photomicrograph(40~) of pelletal phosphorite fromthe Whistler member ofthe Sulphur Mountain Formation at Meosin Mountain. Pellets (black),encased pellet (EP) and nucleated pellet (NP) occurin a carbonate-rich (Cc)matrix.

Photo 13. Photomicrograph (40x) showing a phosphate grain (P) in calcareous siltstone (cross-nicols) from thc Toad Formation. Burnt River area.

Bulletin 98 37 TABLE 6 reaction rims between the carbonate and phosphate are seen QUALITATIVE MINERAL ABUNDANCES IN THE occasionally. Ata locality north of MountLudington, hi Shly TOAD FORMATION PHOSPHATE ROCKS corroded phosphate nodules appear to have been replxed (Determined by x-ray diffraction) by carbonate. ~ ~~ Pelletal phosphorite is relatively rare and restricted to SampleLocation Minerals ldentificd more northerly locations although pelletal phosphorite at Lemoray mayalso belong to the Toad Formation.Pellets are brown to dark brown, 0.05 to 0.15 millimetre in diameter SB87-16(3) Lemoray Fluorapatite >> minordolomite, quartz, and subrounded. More than half of the pellets are nucleated illite with or withouta mixed laycr clay around quartz grains; a few encased pellets are also present. SB87-19(1) LemorayQuartz >> calcite > minorfluorapatite, Where pellets have carbonate cores, textures suggest re- illitc and plagioclase > trace dolomite placement of carbonate by phosphate has taken place. The and K-fcldspar. matrix of these pelletal phosphate beds varies from carbonate rich at Richards Creek to a quartz-calcite matrix with SB87-34(2) MountCalcite quartz? apatite dolomite >> minor feldspar along the Alaska Highway north of the 'Tetsa Ludington trace illite, plagioclase, K-fcldspar. River; some phosphate cement is also present. SB87-35 MountCalcite >> apafite "quartz >> trace Qualitative mineral abundances for these phosphate- Ludingtonillitc. bearing strata are given in Table 6. The presence of apatite SB87-36(1) Laurier Calcite > quartz >> apatite ? dolomitc > ratherthanfluorapatiteinmanyofthesamplesissignifi-ant. Pass minor illite, plagioclase> trace The apatite is most probably present in the matrix and may North K feldspar. represent transported detrital material and not in situ cepo- sition of phosphate. SB87-37(2) Richards Quartz>> calcite> dolomite > apatite Creek > plagioclase A minor muscovite, illite, FERNIE FORMATION K-fcldspar p trace pyrite. The basal phosphate of the Jurassic Femie Formation SB87-37(4) Richards Calcitc >> quartz> dolomite? apatitc is essentially all pelletal phosphorite, although some nodu- Creck >>trace K-fcldspar, illite lar material is present locally at the Crow deposit and Lodge plagioclasc. occurrences. Pellets are brown to dark brown (Photo 14), black, well sorted, subrounded to !mban&r SB87-40 Alaska Calcite > qua~iz> fluorapatite >> occasionally size varying from to millimetre, Ap- Highway minor dolomite> trace feldspar. with a grain 0.1 0.3 proximately 95% of the pellets are structureless and ~p to SB87-43 AlaskaCalcite >> apatitc ? quartz >> minor 50% are nucleated. Occasionally the pellets have an oolitic Highwaydolomite b traceK-feldspar, pyrite. structure. Pellets are composed of fluorapatite and or::anic SB87-43(1) AlaskaQuartz > calcite > fluorapatite > material that gives them their brown colour. The matrix is Highwaydolomitc >> traceK-feldspar,- generally finer grained than the pellets. A general molding

Photo 14. Photomicrograph (100~)in plain polarized light of pelletal phosphorite from the Fcrnie Formation- Crow deposir Semi-compact pellets ocurin a matrixof quartz, calcite and minor clay and mica.

38 Geological Survey Branch Ministry ofEmployment and lnvesfment

Photo 15. Photomicrograph (40x) in plain polarized lightof pelletal phosphorite from the Fernie Formation locatcd at the Lizard deposit. Pellets (P)and nucleated pellets (P) are presentin a dominantly calcite (Cc) matrix.

Photo 16. Photomicrograph (40x) of pelletal phosphorite in the Fernie Formation- Ahby locality. Phosphate pellets (brown)occur in a quartz-rich matrix. Rare pellet is nucleated (NP).

Bulletin 98 39 TABLE 7 of pellets is seen suggesting that their deposition may have QUALITATIVEABUNDANCE OF MINERALSbeen as plastic or gel-like material. PRESENT IN THE BASAL ERNIE PHOSPHATE (Determined by x-ray diffraction) The phosphorite has a compact to semidispersed tex-

~~ ~ ture and contains 50 to 85% pellets by volume. Quam is SampleLocation Minerals Identified the principal component of the matrix except in the Lizard NO. Range - Iron Creek area. Here, calcite is dominant and "" quartzisvirtuallyahsent(Photo15).Thiszonatiouofcalcite Lizard Lizard Lizard Calcite > fluomatite >> quam > albite and quartz has been alluded to in Chapter 3. The variability montmorillonite. mixed clay. 2 of calcite and quartz is very evident in thin sections studied. SBB86-3 Highway3 ' > calcite > quartz > dolomite, albite K-feldspar, illitelse~cite. At the Line Creek deposit and Abby occurrence (Photo16) SBB86-4F Crow->qua& >> k-feldspar, calcite, calciteis virtually absent.Some calcite is present in the illite, albite.illite, Cabin Creek area atand the Crow deposit; feldspar and al- SBB86-11 Iran Calcite > quam > fhwgask >> albite > bite are present in minor amounts, illite, montmorillonite Creek K-feldspar, illite. and sericite are present in trace to minor amounts. Dolcmite SBB86-14Bingay Quartz > K-feldspar > >> albite > is generally absent but does occur locally in @aceamounts. illite. Limonite, probably after pyrite, is usually present in SBB86-I5Zip Fluoramtile >> quartz > minor K-feldspar, amounts of 1 to 2%. The qualitative mineral ahundanws, as illite, montmorillonite * albite. determined by x-ray diffraction on 14 samples is prescnted SBB86-22Harrier Quam > albite > ' >>minor Lakechlorite, illite * trace amphibole. in Table 7. Therelative abundance of the major miner,alsis SBB86-37Barnes->>quartz >> K-feldspar,albite > presented in 21. Lakeuaceillite,montmorillonite. SBB86-38Cabin mc!r@&&> quartz >> calcite > minor Creek K-feldspar. illite * albite montmorillonite. SBB86-42Cabin Quartz > fluw&& >> K-feldspar > minor C reek illite. Creek SBB86-52 Cabin Fluoraoatite >> calcite ? quam >> minor to Creek trace K-feldspar,albite, illite, montmorillonite. SBB86-54Cabin Quartz >> ilm?a&~ > K-feldspar > albite > Creek minor illite > tracemontmorillonite. SBB86-70 Mount Elm&&>> quam > K-feldspar, albite, Lpe illite. SBB86-86Lodge Ehx@lc > quartz > minor K-feldspar, illite. montmorillonite.

40 Geological Survey Branch CHAPTER 5 GEOCHEMISTRY

The geochemistry of phosphate deposits isan important the optimum value. This generally reflects an ovcrall high consideration in the economics of their commercial exploi- clay.content and locally high dolomite content. tation. The presenceof calcite and dolomite adversely affect Sulphur present in phosphate rock may be due to the the beneficiation of phosphate rock by increasing acid con- presence of sulphides, sulphates or organic matter. The most sumption in the acidulation process, the first step in the common sulphate minerals are barite, gypsum and celestite. manufacture of phosphate fertilizers. Conversely, the ability Only barite has been recognized in British Columbia pbos- to recover uranium, yttrium and rare-earth elements as phate deposits. Sulphide minerals are most commonly pre- byprodncts of the acidulation process can provide a substan- sent as pyrite and marcasite. Some sphaleritemay t,epresent tial economic benefit. locally, most commonly in deposits of Triassic ag:. According to Krauskopf (1955) and Gulbrandsen Fluorine may be present in phosphorites in th: form of (1966) the abundance of trace elements or phosphorites is fluorspar or bound toapatite. The F/PzOs ratio characteristic due to their association with organic matter or to integration of fluorapatite varies between 0.08 and 0.12 (Slansky, into the apatite lattice. High concentrations of arsenic, cop- 1986). Ratios for FP2Os for the various phosphate bearing per, lead and zinc are principally due to the presence of or- formations in British Columbia are summarized in Table 9. ganic matter, whereas concentrations of strontium, uranium, Ratios in excess of 0.12 suggestthe presence of fluorite. thorium and rare earths areassociated with fluorapatite. Fluorine is most abundant in the Sulphur Mountain For- From a processing point of viewthe abundance of lime, mation wherevalues generally exceed 2% and int11e Fernie magnesia, alumina and organic carbon are important con- Formation where the fluorine contentaverages 1.43%. Per- siderations. Major element and trace element analyses mian phosphates generally contain less than 2%. analyses for thevarious phosphate horizons in British Co- lumbia are presented in Appendices 2 to5 and 6 to 9 respectively. Results for phosphate and trace elements from the TRACE ELEMENT GEOCHEMISTRY detailed chip sampling are presented in Appendices 10 and Marine sedimentary phosphate deposits generally con- 11. Average for the trace element abundances for some Brit- tain uranium inthe range 50 to 300 ppm, withmost contain- ish Columbia phosphate are compared to the Phosphoria ing less than 100 ppm (Slansky, 1986). It is be ieved to Formation and the “average phosphorite” worldwide in Ta- replace calcium in the apatite lattice (Altschuler etd, 1958) hle 8. and varies directly with phosphate content. Also, it is generally thought that reworking will increase the uranium con- MAJOR ELEMENT GEOCHEMISTRY tent while weathering tends to depleteit. Uranium shows a moderate to strong correlalion with The ideal CaO/PzOs ratio for fluorapatite phosphate grade based on results reported in Appendices 10 (Calo(PO4)6F2) is 1.31. Carbonate may substitute for phos- and 11 (Figure 29). Theuraniumcontent of 16 samples from phateuptoaratioof 1.57.Ratiosgreaterthan 1.57generally the Femie Formation ranged from 1 to 75 ppm (P.ppendix indicate the presence of free carbonate in the phosphate 9) and averages 33 ppm (Table8). Eight samples from phos- rock. Phosphorites in the Fernie Formation show a zonal phatic rocks in the Ishbel Group returned analyses of 4 to distribution of CaO/PzOs ratios. Deposits along the western 103 ppm (Appendix 7), with a mean of 36 ppm (Table 8). margin of the Femie basin exceed the acceptable ratio while In comparison, the average uranium content of the Phos- deposits tothe east and southeast have ratios less than 1.60. phoria Formation is 90 ppm (Slansky, 1986). Ur;mium is Triassicphosphorites in theSnlphurMountain andToadfor- highest in the Whistler member phosphorite generally ex- mations generally have high ratios reflecting an abundance ceeding 100 ppm (Appendix 8). Uranium, based on results of carbonate. Permian phosphates show a wide range of reported in Appendices 10 and 11, shows a moderate to Cao/P205 ratios, but in general they are also unacceptably strong correlation with phosphate grade (Figure X), high. Rare earth contents in phosphorites range from 0.01 to Fertilizer processing plants require an MgO content of 0.15% with marine phosphorites tending to be enliched in less than 1%. Most Femie phosphorite has an acceptable the heavier lanthanides and depleted in cerium. Because MgO content. Whistler member phosphorite has a high these elements can be incorporated into the apatite lattice magnesium content locally as do many of the occurrences they tend to show a strong relationship to the phosphate in the Toad Formation. Better grade Permian phosphate de- grade. While yttrium (Figure 27) and lanthanum (Figure 28) posits have a low magnesium content. Kechika and Road tend to have a strong correlation in British Columt ia phos- River Formation phosphatic deposits are exceedingly high phorites, the correlation between cerium and phosphate is, in magnesium. at best, moderate; the Whistler phosphorite shows ktually The optimum value for the R203/P205 ratio is 0.1 no correlation between cerium and phosphate. Yttrium, lan- (R203 equivalent to AI203 + Fez03 + MgO). Most phos- thanum and cerium are highest in the Fernie phcsphorite phate deposits in British Columbia have ratios that exceed averaging 480,195 and 130 ppm respectively (Tablc 8).The

Bulletin 98 41 British Colurnbia ~.

~ ~~ ~~ ~~~ ~~~~~ ~~~ ~~ ~ ~ ~~

~~~~~ ~~~~~~ TABLE 8 AVERAGE TRACE ELEMENT CONTENT IN PHOSPHATE ROCKS SAMPLED IN THIS STUDY AND AVERAGE VALUES OBTAINED BY GULBRANDSEN (1966) AND ALTSCHULER (1980)

Ishbell Fcrnic' Average Phosphoria Avcragc croup Triassic' Fm. Shale Fm.Element' Shale Phosphorite ("=8) (n=21) (n=16) Ni 42100 63 53 40 Cr 90 IO00 125 53 110 .. Sr 300 3961000 750 785 736 Rb 450 .. .. 4 32 .. Y 1000 480260 121 I 84 13 40 23 40 As 13 3 II <30 Ba 580 Ba 100 350 165497 609 Ag 0.07 3 2 <0.5

TABLE 9 F/PzOs RATIOS FOR PHOSPHATE-BEARING FORMATIONS IN BRITSH COLUMBIA

Permian Triassic Jurassic Sample No. F&Os SampleSample No. F&OI No. FlpzOI

SBB86-X5 0.06 SB87-6 0.06 SBB86-X5 0.08 LIZ 0.06 SBB86-17 0.1 SBB86-3 SB87-7(4) 0.07 0.08 SBB86-41 0.1 SBB86-4 SB87-I l(2) 0.07 0.06 SBB86-57 0.07 SBB86-57 SB87-I2 0.07 SBB86-6 0.06 SBBX6-62 0.09 SB87-15 0.07 SB87-15 0.09 SBBX6-62 SBB86-ll 0.09 SBB86-71 0.07 SB87-16(3) 0.06 0.06 SBB86-13D SBB86-79(1)SBB86-15 0.06 0.16 SB87-19(1) 0.06 SBB86-X4 0.23 0.14 SB87-32 SBB86-22 0.1 SB87-G(I) 0.06 SBB86-37 SB87-32(1) 0.17 0.06 0.06 SB87-34 SBWC(2) 0.06 0.19 SBB86-38 0.08 SB87-34(2) 0.06 SBB86-40SB87-37 I0.06 SB87-34(2) 0.08 SB87-45 0.08 0.09 SB87-35' SBB86-42 0.09 SB87-36 0.9 SBB86-52 0.07 SB87-36(1) 0.08 SBB86-54 0.12 0.07 SBB86-70 SB87-36(2) 0.07 0.06 SB87-37(1) 0.13 0.07 SBB86-86 SB87-37(2) 0.09 SB87-37(2) SB87-37(4j 0.09 SB87-37(4j SB87-40 0.08 SB87-43 0.08 SB87-43(1) 0.08 ___ 42 Geo/ogical Suwey Blanch Ministry of Employment and lnvestment

PERMIAN i ~0.8970 r=0.6588 + i y=4.5634x + 7.2849 v=13.9824x + 35.6851 I + 600 + + ++ + I c

T+ + +

0 0 *++ 5+ 10+ 15 20 725 50L0 5 10 P205 (%) P205 (%) WHISTLER ++ r=0.8353 WHISTLER

+ ++ y=4.5881x + 8.0916 + + ~0.8082 i 5006ooi y=19.1718x + (-14.2608)++ + ++ + + ++ + E + 300 v +++ A + -> ,004 +

+ 4001 t .Oj&+++ ++ ++ + :+ , + , 0 ; I I I .I 0 0 5 10 15 20 25 -7- 0 5 10 15 20 25 P205 (%) P205 (%) FERNIE r=0.7168 t FERNIE

y=1.5239x + 10.9498 + r=0.8622 + y=23,2879x + 31.7521 + + ++ + +++ 60 t +t 800 ++ t + ++ l0O01

+ ;++ ++ + + + ++ +++ +++++ + + ++ + i + + .e +; + # ++++.+ + +$ 400 + ++ 20 +*+ $+ + + + + + + + + ++

+ 40i 2ooJ;y+ ++, 0 ,~ ++ + ++ + .__ ;1 , I 1 + 0 5 10 15 20 25 0 "- L P205 (%) 0 5 10 15 20 25 P205 (%) I

Figure 26. Correlation between uranium and phosphatefor Figure 27. Correlation between yttrium and phosphale for Permian, Whistler member and Fernie Formation phosphates. Permian, Whistler member and Fernie Formation phos?hates. British Columbia __

~ Whistler member phosphorite also contains signifitxnt amountsofyttrium,averaging250ppmoveralland337~~pm PERMIAN in the Wapiti Lake area (Appendix 12). r=0.7771 t + y=8.3959x + 25.0003 Thorium contentin marine phosphatesis generally low, 300 t averaging 6 to 7 ppm (Altschuler, 1980). The thorium (:on- tent ofBritish Columbia deposits approximates the average, E as compared to a mean of 11 ppm in the Phosphoria Fo~ma- 2 200 v ++ + tion. t

4 150 Selenium generally shows some enrichment in phos- + + phorites compared to the average shale and is believed to -2501 correlate with the amount of organicmaterial present. $:ele- nium in phosphorites of the Femie Formation and Ishbel Group varies from 1 to 6 ppm with slightly higher valu8:s in the Ishbel Group. Triassic phosphate deposits vary frcmm 5 P205 (%) to 55 ppm and average 16 ppm. These higher values reflect the higher organic carbon content present in these !:edi- WHISTLER ments. ~0.7676 150 y=5.5143x + (-6.6576) Arsenic in phosphate depositsin British Columbia av- + erages less than 9 ppm compared to a mean of 23 ppm for + + phosphorites ingeneral (Altschuler, 1980). Cadmiurnis also low for all deposits averaging between0.9 and 16 ppnx. Nei- E 100 + v"IQ ther of these metals are present in sufficient quantity to pose any potential health or environmental problems.

The Fernie Formation contains above average vdues

for strontium and barium, 954 ppm and 522 ppm re:,pec- tively, compared to 750 ppm and 350 ppm for the avmage + phosphorite. The highest values for both barium and siron-

0 0 +It+5 *+ 10+ 15 + 20 .725 50Ltium are in the Triassic phosphate deposits, averaging 609 P205 (Z) and 736 ppm respectively. Vanadium showseither a poor or a negative cornel Ition with phosphate grade. With the exception of the Triassic phosphate deposits, vanadium shows no enrichment from average shale. Cadmium.is a toxic metal that occurs inmast phosphate rock. Because of its toxicity new regulations relating to the maximum allowable in the manufacture of fertilizers are now under consideration. All phosphate deposits in British Columbia have below average amounts of this metal with Femie Formation averaging the lowest at 0.9 ppm. Zinc is enriched in Triassic phosphates, averaginl: 695

0 5 10 15 20 25 ppm, compared to both the average phosphorite and shale. P205 (%) Detailed sampling (Appendix1 I) of these deposits returned values in excess of 1000 ppm at four localities. Both the Figure 28. Correlation between lanthanum and phosphate for Fernie and Permian phosphates contain below avcrage Permian, Whistler member and Femie Formation phosphates. amounts of zinc.

44 Geological Survey E'ranch Ministry of Employment ond Investmmt

CHAPTER 6 DESCRIPTION OF PHOSPHATE LOCAILI[TI[ES

PHOSPHATE LOCALITIES IN THE FEMEBASIN Phosphate is present in the Fernie Basinin the Permian Ishbel Group and the Jurassic Fernie Formation. Twenty- nine occurrencesanddeposits aredescribedinthe following section; numbers in parenthesesrefer to numbered localities on Figure 14, in pocket). FORSYTH CREEK - NTS: 82J/2 CONNOR LAKES (I) MINFILE 082JSW029,030 MINFILE Lat: 50O17'50" I1So02'45" Long:

Several exposures of phosphate in the Ross Creek and Ranger Canyon Formations lie north of Forsyth Creek, in the Connor Lakes area. These strata are unconformably overlain by siltstone of the Triassic Sulphur Mountain For- mation (Photo 17). Two sections were measured inthis area (Figures 29and 30). TheRangerCanyon Formation consists primarily of a thick, resistant sequence ofcherts that is overlain by a siltstone bed 1 metre thick containing 10 to 15% black, subrounded phosphate nodules, averaging5 centimetres in diameter (Photo 18). They contain 25.8to 28% P205 but a sample collected across the sandstone bed assayed only 1.6% P2os. A massive to nodular phosphate bed, 0.5 metre thick, underlies the chert bed in the more northerly section (Figure 34). It contains 18.6% &os. It is underlain byaphosphaticinterval, IOmetresthick.With theexception of the uppermost bed, the phosphate contentis less than 5% L Figure 29. Stratigraphic Section62, Forsyth Creek.

Photo 17. View lookin:: north along contact between Permian Ranger Canyon Formation (Rc) and Triassic Sulphur M,,untain Formation (TSR)north of Forsylh Creek. Phosphate-bearing !:iltstone (P) occurs along the upper contact of bedded chert.

Bulletin 98 45 Siltstone: buff weathering. dark grey, resistant. phosphote-probably as Cementond ,ore nodules - 0.20.13.43.26.20.27 Silt~tone:interbedded chert. bull weathering.grey, recessive. medium bedded (5-10 cm: chert-darkgrey to black - <0.10,16,39.22,24,27 - C0.10.9.22.22.14.23 Siltstone: buff weothering,grey, slight, mottled appeorunce, rare phosphatenodules a.30.12.~4,~8,~5.30 Chert: darkQrey to black. recessive - Siltstone-nodularphosphate: siltstone-buff yeathedng, yrey. resirtant: phoEphd? nodules- - t0.10.14.60.28.24.30 grey 10 black. lrregulai shaped, up to 10 cm in size - <0.10.15,33.19.13,28 Cherl: darkgrey to black. receseive, phosphatic <0.10.9,44.18.20.17 - Siltstone: buff weathering,yrey, recesrive: contains few chertand phosphate nodlller - <0.10,14,43,22,26.30

Covered intervol

Siltstone: buff-brown weothering.grey. resistant. thick-bedded to molsive: few phosphaie ovoidnodules (t5X)

SiitEtone: buff-brownweathering. yrey, recessive. Contoins two very thin shalebed9

Siltstone: brownish yrey weathering, grey. massive resistant

Siltstone:brownish grey weathering, yrey. mosoive recessive

Siltrtone: brownishgrey weathering, grey, resirtont. rare phospoFphotenodules

siitrtone L Phosphotic ...... P Figure 30. Stratigraphic Section6, Forsyth Creek

Photo 18. Phosphate nodlles (black) in a 1-metre-thick silt!tone bed overlying chertat the top of the Ranger Canyon Formarion ir. the Connor Lakes areanorth of Forsyth Creek.

46 Geological Survey Brznch Ministry of Employment and 11Wnt

The geologyof this area is complicated by structural Several exposures of phosphate were examincd along thickening due tosteeply dipping normal faults, particularly the MacDonald thrust fault at the southern margin of the in the more northerly section. Several fault repetitions can Fernie basin. Stratigraphic sections were measured at be seen in outcrop. especially in beds beneath the chert ho- Mount Broadwood. northof Fenster Creek andat a locality rizon. Along strike tothe north faulting becomes less preva- approximately 4 kilometres northwest of CabinPa:;s. lent and the phosphatic interval thins dramatically. Low grade phosphate occurs in the basal portion of the The Ross CreekFormation contains a number of sand- Johnston Canyon Formation and canbe traced almost cou- stone beds with phosphate nodules.The nodules are a minor tinuously from the Fernie ski-hill in the northwest o Burn- component of the rock and the phosphate grade islow, av- ham Creek inthe southeast (Figure3 1). It varies in thickness eraging approximately 0.9% PzOs. from less than 1 metre in the Burnham Creek (Section 41) area to 22 metres near Mount Broadwood (Section17). MACDONALD THRUST FAULT (2) NTS: 8260 Phosphate is most commonly present as nodldes, hut M INFILE: Mt. Broadwood Mt.MINFILE: 082GSE069 also as phosphate cement, phosphatic replacementof shell Fenster Creek O82GSE066 material and rarely,as intraclasts. It also occurs as ciasts and Ram South 082GSE067 cement in a thin basal conglomerate that appears tq extend Lat: 49"10'30" to Long: 115"49'05" along the entire length of the fault. Host lithologies 'are typi- 49"18'00" to 114°56'55" cally siltstones and fine-grained sandstones with minor shale. Locally these clastic strata arecalcareous. At Mount Broadwood, where the thickest ph'xphatic interval was observed. individual Dhosohate beds contain

L_1Siltstone Sondstone

conglomerate

Dolomite

Silty dolomite =Shale

Colcoreous Shoie

Chert nodule9 .,...... Phosphatic...... P ..... Covered intervol ...... CI ...... % P205...... 1.23 ...... PEYRMIAN

Y Y Y "z JOHNSTON c1 CANYON I FORMATION CANYON FORMATION I CI

TRIASS

i"i...... unconformit- .E?- ...... KANANASKISFORMATION PENNSYLVANIAN phoaphatic c00"glorn:role 2 ~rnthick _" KANANASKISFORMATION 1 PENNSYLVANIAN

Figure 31. Stratigraphic correlationof phosphate-.hearing strata, Johnston Canyon Formation, Fernie ski-hill-Cabin Creek area.

Bulletin 98 47 British Columbia __

0.2 to 2.66% P205. Phosphate is typically nodular (Photo FERNIE SKI-HILL (3) NTS: 82Gf6 19)althoughitisalsopresentascement.Thebasalconglom- MINFILE: 082GSW360 erate, which is 30 centimetres thick, contains 3.20% Pz05. Lat: 49"27'40" Long: 115"06'20" At theFensterCreeklocality, clastic beds aremorecal- careous and containrelatively abundant bioclastic debris. A In the Lizard Range, andspecifically at the Fernie ski- calcareous sandstone bed 0.5 metre thick contains 11.70% hill, Permian strata are overturned. This locality provies the P20s. Thebasal conglomerate contains 4.0% Pzo5. rare opportunity to measure a section across the entire Per- Near Cabin Pass only nodular phosphateis present and mian sequence (Figure32). The Johston CanyonFormaion individual beds contain less than 2% Pz05. is approximately 100 metres thick and contains a few very Nodular phosphatic beds of the Ranger Canyon Forma-thin phosphatic shale beds in the upper part of the section. tion may also be present locally. The basal conglomerate, which occurs throughout the region, is represented by a bed only 21 centimetresthick. The Ross Creek Formationis approximately 25 metres thick and contains three rare very low-grade phosphatic shale beds. The author has placed these strata in the Ross Creek Formation. This designation is far from certai,l as these beds may be part of the underlying Johnston Ceek Formation or the overlying Ranger Canyon Formation. The Ranger Canyon Formation as defined here is approximately SO metres thick and consists of chert and sandstone. Close to the top there is a phosphate bec. 50 centimetres thick containing 13.30% P2O5 (Photo 20). Phosphate is present as nodules, pellets and cement. The nodules may contain quartzgrains and chert spicules or may be devoid of any extraneous material. The phosphate bed itself is composed of quartz, potash feldspar, minor i ilite, sericite, calcite and albite and is underlain by phosphatic sandstone and chert. WEIGERTCREEK (4) NTS: 82Wl5 MINFILE 082GNEO38,039 Lat: 49'51'45" Long: 114°SC:25"

Johnston-Canyon Formation, Mount Broadwood. Phosphate is exposed at two localities along a four- wheel-drive road that extends northward from the main

Photo 20. Phosphorite bed from the topof the Ranger Canyon Formation, Fernic-ski-hill

.__ 48 Geological Survey 6 ranch Ministry of Employment and Ifivestment

0.64 0.19

0.08

1.04 6 45 46 29 44 1.65'735h6$4>54 1.53:3.55,49.38.41

Figure 32. Stratigraphic section 8, Fcrnie ski-hill.

Bulletin 98 49 Photo 21. Photomicrograph (40x) of pelletal phosphorite from the Johnston Canyon Formation,Weigert Creek Phosphate pellets (P) and nucleated pellets (NP) occurin a calcite (Cc)quartz (Q) matrix.

Photo 22. Pelletal phosphorite from the Johnston Canyon Formation,hcadwaten of Nordstrom Creek. Weigert Creek logging road north of Sparwood. It is inter- cherty limestone bed 10 centimetres thick. The ba:;al2rne- preted to occur alongthe limbs of a north-trending anticlinal tres of thephosphatic sequence averages 23.2% P205 and is fold in the Johnston Canyon Formation. Lithologies include overlain by 1 metreofinterbeddedshaleandphosphate,than sandstone, shale, dolomitic siltstoneand conglomerate. a bed of lower grade phosphate, 90 centimetres thick, con- The western exposure consistsof a phosphorite bed 2 taining 13.4% PzOs, and capped by 2 metres of phosphatic metres thick averaging 14.25% PzOs and comprised of semidispersed, subrounded, generally structureless pellets shale with a phosphate content averaging less than 5% P205. (Photo 21). Approximately 5% of the pellets arenucleated and a very few are oolitic. Some phosphate cement is also present. The pellets, which comprise 40 to50% of the rock by volume, occur primarily in a quartz matrix with some feldspar. The eastern exposure consists of a phosphorite bed 1 metre thick containing 15.8% PzOs (Photo 37). The phosphorite is pelletal, with the pellets comprising 50 to 60% of the rock by volume. They are subrounded, brown to dark brown, with a grain size of 0.1 to 0.5 millimetre. Less than 5% of the pellets arenucleated or encased. Rare oolitic radial structures may also he present. The matrix is comprised mainly of calcite with minor quartz and clay minerals.

NORDSTRUM CREEK (5) NTS: 82Gl15 MINLlLE 082GNE037 Lat: 40"51'50" Long: 11439'55''

Three phosphate beds are poorly exposed over a 60-metre width near the headwaters of Nordstrum Creek southwest of Fernie, at the end of a seismic survey line. The area between the phosphate beds is covered by overburden. The host rocks are buff-brown-weathering sandstone and pale grey quartzitic siltstone of the Johnston Canyon Formation. The most westerly bed has an exposed thickness of 1 metre and contains 21.20% P20s as nodules, pellets and cement (Photo 22). The matrix consists of quartz, bioclastic debris and minor feldspar. The two easterly beds contain approximately 5% phosphate nodules by volume and less than 2% PzOs. The nodules are composed of fluorapatite, quartz, and minor dolomite and potash feldspar. Both of the beds are 1 metre Figure 33. Location of phosphate horizon in the Line Cr(zk area. or less thick.

~~~~ ~ LINE CREEKLINE (6) NTS: 82G/15W Line Creek MINFILE 082GNE028 Hamet Lake 082GNE030 49"YOO" Long: 114"48'00" Long:Lat: 49"YOO"

Cominco Ltd. owns six phosphate leases in the West Line Creek area in the Wisukitsak Range, east of the Elk River. A phosphate horizon varying in thickness from less than 1 metre to in excess of 3 metres occurs at the base of the Fernie Formation. It can be traced along strike for 15 kilometres (Figure 33); 8 kilometres of strike length are covered by the Cominco leases. A steep, easterly dipping phosphate sequence 4.9 metres thick is exposed on Mount Lyne, site of Cominco's bulk sample (G.L. Webber, personal communication, 1.986) (Fig- ure 34). The base of this sequence is marked by a marcasite hand 5 centimetres thick and the top by a yellow-orange Figure 34. Stratigraphic section,70, Mount Lye.

Bulletin 98 British Columbia .~

The phosphorite at Mount Lyne is typically pelletal with a compact (Photo 23) to semidispersed texture. The A A' 1 pellets arechestnut-brown todarkbrown,ovoid, moderately (19.50% P205/1.75m) well sorted and generally structureless. Less than 5% are nucleated. The matrix is comprised almost entirely of quartz, with trace amounts of sericite and illite. Neither petrographic nor x-ray diffraction work reveals the presence of 2000 any carbonate. Between the Line Creek access road and Mount Lyne, 1800 Crows Nest Resources Ltd. obtained values of 3.7% P205 in 8' a diamond-drill hole and 23.7% P205 across 1.6 metres in a backhoe trench (Hannah, 1980). The phosphate bed dips be- I tween 45 and 70" east throughout its strikelength (see Fig- ures 33 and 35). Along strike, a distance of approximately 11 kilometres from Mount Lyne to the south, near Harriet Lake, this phosphatic interval thins to 85 centimetres and 1800 contains 13.8% PzOs. CROW (7) NTS: 82G/10 1600 MINFILE 082GNE025 Lat: 49"39'45" Long: 114"42'30" Long: 49"39'45" Lat: (23.71% P205/1.6m)

TheCrow property, consistingoffour phosphate leases, Bock-hoe trench is located at the west end of the Crowsnest Pass, 2.5 kilo- 1800 metres north of the gas pipeline pumping station on High- way 3 (Figure 14). Phosphorite was discovered by 'ielfer at 1600 the base of the Fernie Formation in the early 1900s. Explo- Creek ration continued intermittingly until the mid-1970s by the D D' Consolidated Mining and Smelting Company of Canada, 1700 7 Line Creek Road Limited (now Cominco Ltd.). During this time they completed 600 metres of underground work and shipped an 1800-tonnesampletoTrailformetallurgicaltestingin1931. Further testing was done in the mid-1960s. Beneficiation 1300 work by Cominco has yielded acceptable concentrate \ Phosphate bed .....- grades with recoveries of approximately 75% (Kenny, 0 1977). Modifiedfrom HANNAH (1980)

Figure 35. Cross-sections through Fernie phosphate, West Line Crcck.

52 Geological Survey BrLnch Figure 36. Cross-section through the Crow deposit (from Telfer, 1933).

The adit and underground workings are now inaccessi- ALEXANDERCREEK - NTS::82G/lO ble. Only one old trench and a few surface exposures south HIGHWAY 3 (8) of the underground workingsare available for examination. MINFILE AlexanderCreekSouth08LGNE029 Telfer (1933) describes the phosphate horizon as consisting Highway 3 Roadcut 082:3NEO33 of threebeds: a lower oolitic high-grade phosphorite,a shale parting and an upper nodular phosphorite with a yellow Lat: 4Y39'15" Long: 11~1"44'10" marker bedat the top. The high-grade phosphorite bedcon- sists of structureless pellets and rare pellets with an oolitic Aphosphoritehed1.2metresthickisexposedinaroad- texture. The beds average approximately 1 metre in thick- cut on Highway3 near Alexander Creek (Figure 37) uncon- ness, hut arerepeated as manyas four or five times byeast- formably overlying shale and siltstone of the Sulphur erly directed thrusting (Telfer, 1933).

~~ Telfer describes a section through an inclined shaft at ~ ~~~ the southern endof the underground workings wherestack- No\*: sequnul *I Chaniuli onohvr is h0. * li ". V. 1, La. cs YI Rm ing offault slices has compressed almost100 metres ofdip- length to less than 40 metres (Figure 36). The resulting thickening of the phosphorite beds extends over a strike length of 150 metres. Similar structural thickening occurs at the northern end of the exploration drift and midway along the workings whereit isassociated with a 90" change in strike direction. A raise at this point shows the thickening extends 150 metres up-dip beforethe beds resumetheir normal thickness and continueto the surface. The southernmost area of structural thickening can be seen in the old trench above the workings. The phosphate horizon is exposed over an interval of 19 metres within which aphosphorite bed 1 metre thickis repeated fourtimes. Sampling from this trench indicates an average phosphate content of 26.20% PZOS, with 757 ppm yttrium, 319 ppm lanthanum, 183 ppm cerium, 1288 ppm strontium and 41 ppm uranium (Table IO). The phosphate horizon, although not seen in outcrop, is believed to becontinuous into the headwaters of Alexan- der Creek where itis exposed in tworoadcuts. The top and %*Vi ...... ,.,,I bottom ofthe phosphorite are covered, but ithas a minimum thickness of 30 centimetres and assays from2'1.4 to 29.4% Figure 37. Stratigraphic section 3, Highway3 roadcut, PzOs. Bedding in this area dips westat approximately 25". approximately 8 kilometres eastof Michel.

Bu//elin98 53 British Columbia __

TABLE 10 ANALYTICAL RESULTS, CROW DEPOSIT

~~ ~~~~ ~~~ Samplc Width PzOs -~ ~ ~~ ~~~~ Number (metres) (%) Sc Cu Pb Zn Sr Y U Th V La Ce Ti Ba

SBB86 4A 20 1.0044 2.3 6.6 200 12689 <61214 32 485 1253 116 929 SBB86 40 1.00 6.6 3.3 41 22 180 1290 38946 5 94 406 244 939 :398 SBB86 4C 1.00 25.7 3.6 27 40 241 1293 42946 91 2 409 222 935 387 SBB86 4D 1.00 25.1 2.6 25 40 175 1307 792 905 <6 332 205 85 739 SBB860.70 4E 27.0 2.8 40 22 108 1337 50617 94 <6 247 126 1248 135 "

Avcragc 2.9226.2 0.94 41 23 166 <6 1288 41 757 319 92 183 IO12 !318 "

Mountain Formation. The phosphorite is overlain by phos- The Marten phosphate occurrence is in the valley of phatic shale, minor limestone and shale). Michel Creek, approximately 8 kilometres south of McGil- The phosphorite consists of brown to dark brown, livray station. Exploration by the Consolidated Mining and subangular to subrounded, structureless pellets 0.1 to 0.3 Smelting Company of Canada, Limited in the early 1030s millimetre in diameter. Approximately 5% of the pellets included some underground work. A phosphorite bed at the have nuclei of either quartzor calcite. The pellets are com- base of the Fernie Formation has an average gradeof 1:'.2% P2O5 across 1.9 metres and has been traced along strik:: for pact to semicompact and sometimes molded around previously formed pellets, suggesting that they were in a approximately 1200 metres (J. Hamilton, personal conlmu- gel-like statewhen deposited. The matrix consists of quartz nication, 1986). The bed is reported to strikenortherly with and calcite in equal amounts, with minor dolomite, albite, moderate easterly dips. potassium feldspar and trace illiteand sericite. SUMMIT LAKE (IO) NTS: 82G/,!OW A second phosphate occurrence outcrops along Alex- MINFILE 082GN1?035 ander Creek south of the highway. A phosphorite bed 1 me- Lat: 49"39'10" Long: 114'42'30" tre thick overlies a conglomerate5 centimetres thick at the base of the Fernie Formation (Figure 38). The phosphatic A 3-metre section of Permian strata is poorly exposed section is 5.5 metres thick, its upper limit marked by a yel- on the western boundary of the Crowsnest Provincial :'ark, lowish orange weathering limestone bed 3 centimetres 0.5 kilometre north of Summit Lake. This section represents thick, Shalecut by numerous minor faults overlies the phos- a condensed stratigraphic sequence and is tentative1,y as- phatic sequence. signed to the Johnston Canyon Formation. It overlies Kananaskis or possibly Tunnel Mountain strata of Permian MARTEN (9) NTS: 82GflOW age. MINFlLE 082GNE027 Phosphate is present as nodules in a sandstone bed 1 Lat: 49"34'W Long: 114"47'00" metre thick. Nodules are 2 to 5 centimetres in size, Mack and contain27.5% P205.A sample across the sandston: bed assay 14.5% 405. This same bed is believed to continue south to the Flathead area and northward to Banff. **& i"*_/ LIZARD (11) NTS: 82GIIIE

Sbk I",Y. my "WW. "7 nsirtmli mer mi00 MINFILE 082GSW059 II <*,L;~-me n"mm ar i*nor ,*"ill Lat: 49"29'22" Long: 115"07'40"

TheLizardproperty, consistingoftwo phosphate leases held by Cominco Ltd., is located on Lizard Creek 5 kilometres southwest of Fernie (Figure 14). Only two caved adits and a dump are available for iuspection. The area is over- grown by dense alder and thick underbrush with almost no outcrop. Work by Cominco has indicatedthe presence of a phos- . phorite bed averaging 12.90% Pz05 across 3.4 metre; (Ta- :z -*,is .,...... P n plin, 1967). In thinsection (Photo 15) thephosphoriteis seen Figure 38. Stratigraphic scction31, Alexander Cntik at to consist of brown to dark brown pellets averaging 0.2 to Highway 3. 0.3 millimetre in diameter. They are generally well rollnded

~~ 54 Geological Survey llranch and structureless, with approximately 50% having a qualtz FAIRY CREEK (13) 82G/IIE nucleus. The matrix, which comprises 20% of the rock, is MINFILE 082CiNW054 dominantly carbonate with lesser quartz and minor amounts Lat: 49'32'02'' Long: 11:1"04'55" of mica and clay minerals. Most of the carbonate matrix is the same grain size as the phosphate pellets. Deposition of A phosphatic interval 4 metres thick is exposed nearthe phosphate as a gel evidencedis by molding of pellets around top of the Ranger Canyon Formation on Fairy Creel: (Figure each other. In thin section there isno evidence that the phos- 14). The upper 2 metres average 1.35%Pzos; the lower 2 phorite has been subjected to any significant weathering and metres average 0.32% P205. Phosphate occurs as ovoid upgrading of the phosphate content. nodules and very thin partings of massive pbosphrk along bedding planes. MUTZCREEK ANDUPPER NTS: 82G/IIE ISLANDLAKE (14) 82G/7NTS: MUTZ CREEK (12) MINFILEIsland Lake Two 082GVW031; MINFILE 082GNW055.068 Island Lake One 082C~NW034 Lat: 49"30'40" - 49'36'02'' Long: 115"05'00" Lat: 49'3 1'30" Long: 115°10'40"

An overturned sequence of Mississippian to Jurassic Two phosphate occurrences are exposed in partially rocks is exposed at several localities along a road slumped trenches along the powerline in the Iron Creek - that par- Island Lake area, west of Fernie (Figure 14). The trenches allels Mutz Creek (Figure 14). Phosphatic chert and nodular are believed to have been put in by Crows Nest Rt:sources phosphatic sandstone occur in two beds 40 to 50 centimetres Limited while exploring for phosphate in 1966. At both 10- thick and IO to 20 centimetres thick separated by 1 to 2 calities a phosphorite bed 1 metre thick, with phosp late val- metres of a brownish weathering nonphosphatic sandstone. ues ranging from 13.2 to 15.4% P205, occurs at thr: base of These strata are assigned to the Permian Ranger Canyon the Fernie Formation. The phosphorite is pelletal w. th a ma- Formation. Phosphate nodules weather a distinct white col- trix of calcite and lesser quartz. Minor albite a1d trace our and stand out in relief on weathered surfaces (Photo 24). amounts of potash feldspar and illite are also present. A sample across40 centimetres contained 0.53%Pz05. This HARTLEY LAKE(I.5) phosphate interval islocated 25 metres below the base of a WTS: 82G/II MINFILE 082CNW030 sequence of brownish weathering siltstones and shales of Lat: 49"36'05" Long: 11!i"04'30" the Triassic SulphurMountain Formation. In the same area within the Fernie Formation, a 3. I-me- A phosphorite bed 50 centimetres thick is ex?osed at tre interval of phosphorite and phosphatic shale is exposed the base of the Fernie Formation in an overturned sequence above a conglomerate that occursat the base of the Fernie. exposed on a cliff face overlooking Hartley Lake (Figure The phosphate interval averaged only 0.68% P2O5 . 14). The phosphorite is pelletal, dark grey to black, reces-

Photo 24. Phosphate nodules (white)in a brownish weathering sandstone, Ranger Canyon Formation, Upper Mutz Creek.

Bulletin 98 55 sive, and weakly calcareous; it grades 21.5% PzOs andalso than 5% of the pellets are nucleated (generally qu;lrtz contains 141 ppm vanadium, 160 ppm lanthanum and 84 grains). The occasional pellet is oolitic. The matrix is com- ppmcerium. Stratigraphically underlying the phosphorite is prised of subangular quartz grains with trace to minor a black dolomitic siltstone of the Triassic Sulphur Mountain amounts of potash feldspar, sericite and carbonate. The;>el- Formation. lets comprise 50 to 60% of tbe rock by volume and are semicompact to dispersed. LLADNER CREEK(16) NTS: 82G/lOW The phosphatic sandstone contains 10 to 15%fluorr.pa- MINFILE: 082GNE034 tite pellets. The pellets are subrounded, brown and iiis- Lat: 49"41'40" Long: 114"56'10" persed. Quartz with minor carbonate and trace feldsyr, sericite and carbonate comprise the matrix. Quartz grains Fine siltstonesof the Ranger Canyon Formation are ex- are subangular and moderately well sorted. posed in a roadcut west of Lladner Creek (Figure 14.). This sequence includesthin chert beds and a siltstonebed 50 cen- BINGAY CREEK (18) NTS: 82J/2 timetres thick containing black phosphate nodules. The MINFILE 082JSEDll phosphatic bed can be traced along strike for 40metres and Lat: 50"12'00" Long: 11 5"OO'OO" contains 4.2% P2O5. This phosphate occurrence is located on Bingay Crcek, ABBY(17) NTS: 82J/7 2.4 kilometres upstream from the Elk River forestry road, MINFILE 08USEO16 19 kilometres north ofElkford (Figure 14). Vertical-dipldng Lat: 50"18'25" Long: 114"56'05" conglomerate, phosphorite, sandstone and shale of the Fernie Formation unconformably overlie silty dolomite of The Abby Occurrence is located along the Elk River the Whitehorse Formation (Figure 40). The phosphatic~se- forestry road 31.5 kilometres north of Elkford (Figure 14). quence consists of a phosphorite bed 1.04 metres thick c.on- It is exposed in a trench put in by Cominco Ltd. while ex- taining 11.80% P205, phosphatic sandstone and shale. 'The ploring for phosphate in the mid-1970s. phosphatic sequence is marked by conglomerate (4 centi- Clastic rocks of the Fernie Formation unconformably metres thick) at its base andis capped by an orange-wexth- overlie dolomite and dolomitic siltstone of the Whitehorse ering calcareous bed, 2 centimetres thick. The phosphorite Formation. The base of the Fernie consists of a thin bed of is pelletal and contains a few shell fragments. phosphatic sandstone, overlain by a phosphorite bed 1.5 metres thick (Figure 39) which is in turn overlain by a phos- ELKFORD SKI-HILL (19) NTS: 82J/2'W phatic shale cut by a fault. A 1.0-metre phosphorite bed MINFILE: 08WSE117 overlies the fault zone and is probably a repetitionLong: 50"01'30" of the Lat: 114"57':10" lower phosphorite bed. The phosphorite is pelletal with an average grain size of 0.1 millimetre. Phosphate content of An overturned section of Ishbel Group and Sulphur the two beds averages 20.18%P205; the sandstone averages Mountain Formation strata is exposed immediately absve 3.81% PzOs. Phosphatic shale and shale overlie the phos- the chairlift on the Elkford ski-hill. This locality was bricfly phorite. A 1.O metre sample from the overlying shale unit explored by Cominco Ltd. while exploring for phosphate returned a valueof 26.63% PzO5. along the Elk River valley. In thin section the phosphorite is seen to consist of light A phosphorite bed 50 centimetres thick is exposed mar to dark brown, generally structureless subangular to sub- the base of the Ross Creek Formation (Figure 41), over:ain rounded pellets 0.1 to 0.2millimetre in size (Photo 16). Less by40 centimetres ofphosphatic sandstone. A thinbasal con-

__ Figure 39. Stratigraphicsection 13, Abby Ridge. Figure 40. Stratigraphic section 14, Bingay Creek.

56 Geologicul Survey Brcnch murian age. The phosphate sequence isconformably overlain by belemnitic shales of Toarcian age and underlain unconformably by siltstone and minor shale of the Sulphur Mountain Formation (Figure 42). The phosphorite bed is 80 centimetres thick md contains 19.10% PzOs. It isoverlain by 74 centimetres sf phosphatic shale containing 6.64% PzOs. Similar results were obtained by Cominco in the adit where a pellet31 phosphorite bed 1.2 metres thick containing PzO: is over- PhO*h.ix ...... s 21.3% lain by 51 centimetres ofphosphatic shalecontaining 6.5% PzOs (Wehber, 1975). The phosphorite is typicall) pelletal Figure 41. Stratigraphic section80, Elkford ski-hill. with pellets of fluorapatite present in a matrix of calcite and lesser quartz. glomerate separates the phosphate sequence from limestone of the Telford Formation. The phosphate sequence is over- A diamond-drill hole completed by Cominc o to the lain by siltstone and argilliteof undetermined thickness. northwest, intersected 1.76 metres of phosphate ccotaining The phosphorite is composed of semicompacted ovoid 18.57%P20satadepthof49.4metres(Webber,1976).This pellets, 0.1 to 0.6 millimetre in size with rare compound phosphate horizon is believed to be present west ,>fGrave pellets and oolites (Photo 25). Gangue minerals include Creek area where drilling by Cominco Ltd. intersected 1.5 quartz and calcite. A sample across the phosphorite bed con- metres of phosphate containing 16.93% P'205 (Wehber, tained 5.93% PzOs. 1976). FORDING RIVER (20) NrS: 82645 MINFILE 082GNEO24 Lat: 49"54'20" Long: 114"50'55"

The Fording River phosphate occurrence, which has been known for a number of years, has heen explored by both Crows Nest Resources Limited and Cominco Ltd. Work by Cominco included mapping, trenching and a 12- metre adit. A gently southwest-dipping pelletal phosphorite bed occurs at the base of the Femie Formation and is overlain by phosphatic shale and limestone. These strata are of Sine-

Photo 25. Hand specimen of basal Fernie phosphorite, Lodge phosphate occurrence. Irregular-shaped phosphate nodulcs occur in a pelletal phosphate matrix. _" BuNerin 98 57 BARNES(21)LAKE 82G/7NTS: ZIP (24) NTS: 82U7 MINFILE PH 082GSE038; WW 082GSE051 MINF'ILE 082GSEI64 Lat: 49"27'10" Long: 114"40'50" Long: 49"27'10" Lat: Lat: 49"16'05" Long: 114"36'00"

A phosphorite bed 0.8 to 1.2 metres thick is exposed at The Zip phosphate occurrence is located on Mcrris the base of the Fernie Formation on the limbs of a series of Creek northwest of the junction of the Harvey C!reek and northerly plunging folds in the Barnes Lakes area (Figure Corbin logging roads (Figure 14). This locality was ex- 14). It unconformably overlies siltstone of the Sulphur plored by First Nuclear Corporation Ltd. in 1980; work <:on- Mountain Formation and is overlain by paper shales of the sisted of geological mapping and trenching (Hartley, 1?8l, middle Fernie Formation. Exploration work by Western 1982). Warner Oils Ltd. andMedesto Exploration Ltd. consisted of A phosphorite bed, 0.7 metre thick, is exposed at the geological mapping, trenching, seismic surveys and drilling base of the Fernie Formation and unconformably ove1.1ies (Dorian, 1975; Pelzer, 1977; Dales, 1978) and outlined dolomite and silty dolomite of the Sulphur Mountain ::or- 262 OOO tonnes of phosphorite to a depth of 18 melres (60 mation. It has been repeated several times by thrust faulting. feet). Phosphate grades in surface trenches were reported as Vanadium-rich shales overlie the phosphate (Hartley, 1981). 27.0 to 33.0% P2O5. A sample taken by the author assayed 22.4% Pzo5,452 ppm yttrium, 24 ppm uranium, 198 ppm The phosphate at this locality has a very limited strike lanthanum and 135 ppm cerium across 80 centimetres. length as the Fernie Formation has been truncated IIY a trachytic syenite and the Flathead fault. Based on two sam- Nodular phosphate is also present in sandstone in the ples, phosphate grades are in the range 23.9 to 27.1% F'z05 Johnston Canyon Formation. The phosphate-bearing sand- across a thickness of 0.7 metre. stone bed is 30 to 40 centimetres thick with a phosphate content of 1.7% Pzo5. CABIN CREEK (25) NlX: 82G/2 MINFILE Cabin, CS 082GSEO55; LODGEPOLE (22) NTS: 82G/7W Ram 082GSEO56; Bighorn 082GSE1160; MINFILE 082GSE062 Storm Creek 082GSE061; Ram A 082GSW63; Lat: 49"18'50" Long: 114"55'30" Cabin G 082GSE:068 Lat: 49"06'40" Long: 114"40'45" Long: 49"06'40" Lat: The Lodgepole phosphate Occurrence is located immediately east of thejunction of the Lodgepole and Ram Creek Exploration for phosphate in the Cabin Creek area be- Forestry Roads south of Morrissey (Figure 14). Phosphate gan in 1978 whenImperial Oil Ltd. completed a program of from this area was first reported by Telfer (1933) and has geological mapping and drilling (Van Fraassen, 1978). In seen only minor exploration. MacDonald (1985) also re- 1982FirstNuclearCorporationLtd.reassessedthepotential ported the presence of phosphate-bearing strata in the lower in the area, completing radiometric surveys, geological Fernie Formation at this locality. mapping and trenching (Hartley, 1982). The only exposurefound during this study is a 12-cen- The Cabin Creek area covers the southern limit of the timetre phosphorite bed occurring between two limestone Fernie hasin and the southernmost exposures of phosrhate beds at the base of the Fernie Formation. This phosphorite in both Permian and Jurassic strata in southeastern Blitish was previously described by Freebold (1969) and contains Columbia. A total of 18 phosphatic sections were measured 14.3% PzOs. Thrust faults and small-scale folds are com- by First Nuclear Corporation, some of which were re-exam- mon in the area. ined in the course of this study. Permian strata are represented by the Ranger Canyon LODGE (23) NTS: 82G/7 Formation above and belowthe MacDonald thrust fault and MINF'ILE 082GSEO57 the Johnston Canyon Formation above the fault (Figure 43). Lat: 49"16'50" Long:114"47'40" Phosphate in the Johnston Canyon Formation is typixlly nodular with occasional pelletal phosphate present in a The Lodge phosphate occurrence is located immedi- lower, dark grey to black, calcareous siltstone unit. The ately south of the Lodgepole forestry road, 31 kilometres pelletal phosphate consists of dispersed pellets, 0.3 to 0.5 southeast of Fernie (Figure 14). Exploration for phosphate millimetre in diameter, in a matrix of calcite and qlartz. in this area was done by Imperial Oil Ltd.A phosphorite bed Phosphatized shell material is also present. A thin phos- occurs in brown and blackshale and siltstone atthe base of phatic conglomerate marks the base of the Johnston Caoyon the Femie Formation. These strata unconformably overlie Formation. fine siltstone of the Sulphur Mountain Formation. The only Phosphate is present in the Ranger Canyon Formation outcrop of phosphate is strongly weathered and the thick- in a basal chert-pebble to cohbleconglomerate (Photo5)and ness of the phosphorite was not determined. A large grab as pellets or nodules in the upper part of the section. Uithin sample assayed 29.5% P205. In hand specimen the phos- the conglomerate phosphate occurs both as phosphate peb- phate is both pelletal and nodular (Photo 25). Drilling inter- bles and as cement. The conglomerate, in the one outcrop ested 2.44 metres of phosphate averaging 17.33% Pzo5 examined, is in excess of 2metres thick and includes a 60- (Heffernan, 1978). centimetre section at the top containing 9.58% 1'205. Only

58 Geological Survey Branch Figure 43. Geology and phosphate deposits in the Cabin Creek area minor phosphate is present in the upper part of the Ranger number of localities throughout the Fernie hasin (New- Canyon Formation. march, 1953; MacDonald, 1985). To the north of his locality, at the headwaters of a tributary the Storm Creek, the In the same area, the phosphate horizon inthe basal part of phosphorite bed thins to 1 metre with a phnsphae content of the Fernie Formationis exposed at several localities (Fig- of only 14.0% P205. Here, the phosphorite is strongly ure 48). A phosphorite bed averaging 1.5 metres thick and weathered and contains 2 to 3% limonite. Furtler to the consisting of compact to semicompact pellets (Photo 26), north, west of Hunger Lake, the-phosphorite is atleast 1 outcrops along a strike length of approximately 27 kilome- ~ tres. The pellets are typically subrounded to subangular, structureless, well sorted and 0.1 to 0.3 millimetre in diameter. Less than 2%of the pellets are nucleated. There has been some molding of pelleu, suggesting deposition in a gel or plastic state. The matrix consists of quartz, calcite, minor potash feldspar and trace amounts of albite, dolomite and illite. Although subordinate to quartz, calcite may he abundant locally. The average phosphate content based on sampling at eight localities is 16.8% PzOs and 272 and 188 ppm lanthanum and ceriumrespectively (Table 1 I). In the measured section (Figure 44) two phosphorite beds are separated by a thin brownish colonred shale that may have a substantial bentonite component. The presence , _" of bentonite in the FemieFormation has been reportedat a Figure 44. Stratigraphic section38, Cabin Crfek.

Bulletin 98 59 British Columbia __

Photo 26. Photomicrograph (40x) of pelletal phosphorite from thc Fernie Formation, CabinCrcck area.

~ ~~ ~~~~ ~

~~~ TABLE 11 ANALYTICAL RESULTS CABN CREEK PHOSPORITE

SBB8637A 0.8 22.4 4s 22 144 781 452 24 9 74 198 135 2181 230 SBB86-38A I 18 37 25 204 602 596 43 I5 89 238 149 2049 387 SBB86-38C 0.6 9.99 2SO 41 I500 620 513 80 9 313 313 359 2591 689 SBB864OA 1.2 15.7 28 13 134 330 453 45 7 93 20s 122 2511 323 SBB8b42A I 18.4 28 I1 91 512 520 56 13 92 230 I51 2461 968 SBB8642B 1 18.6 25 23 62 491 534 61 I 95 224 136 2470 Si8 SBB8643A 1 22.2 40 20 175 565 659 81 29 108 295 199 1928 840 SBB8644A 1 27.5 31 16 1IO 47 I 906 66 17 78 413 229 I290 231 SBB86-52A I 14 30 IS LIS 365 415 48 15 85 196 147 2470 3%1

AVerSPe 114 0.951357 18.5356 561 52621 282 257 I81502 2217 metre thick. A grab sample from this locality assayed 29% SHEEP MOUNTAIN (26) NTS: 82G/.!SW P205. MINFILE 082GNEO36 Phosphate within the Fernie Formation occurs both Lat: 49'51'55'' Long: 114°47'10" above aosphorite varies in thickness between 1 and 2 metres and assaysfrom 18.4 to 27.5% PzOs. Above the fault the A thin sequence of Permianstrata, unconformably phosphorite is 1 metre thick with a grade of 9.51% P2O5. overlying dolomitic siltstone of the Pennsylvanian Kananaskis Formation and tentatively assigned to the Workby FirstNuclearCorporationLtd. inthefiumham Johnston Canyon Formation outcrops 500 metres eest of Creek area, south of Cabin Creek, indicated the presence of Harriet Lake (Locality 6A, Figure 14). A phosphat:-ce- phosphorite with grades in excess of 29% P2O5 (Hartley, mated Chert-PebbIe conglomerate, 10 to15 centimmes thick, containing 13.8% P205 marks the contact betxeen 1982). MacDonald (1985) also obtained grades in excess of Pennsylvanian and Permian Strata, The conglomer;,te is 29% P2Os in this =ea as well as in the Storm Creek area. overlain by a phosphatic cherty sandstone bed 70 cen:ime- These localities were not examined by the author. tres thick that contains 0.7% P205.

60 Geological Branch Survey NORTH SULPHUR CREEK (27) NTS: 82G/lIE MEOSIN MOUNTAIN (30) NT!;: 931/8 MINFILE 082GNW069 MINFILE: 0931020,021 Lat: 49"44'25" Long: 115"02'50" Lat: 54"17'00" Long: 120"19'00"

Strata of the Permian Ishbel Group outcrop over a wide Exposures of the phosphate-bearing Whistler member area in the Sulphur Creek area 15 kilometres north of Har- of the Sulphur Mountain Formation are exposed, together tley Lake (Locality 15, Figure 14). Nodular phosphatic ma- with other Triassic and Permian strata, on the eastern flank terial is present in both outcrop and talus over much of this of Meosin Mountain (Figure 16). Two sections measured in area. this area show that a phosphorite bed near the ba;e of the Also at this locality a 90-centimetre-thick coquinoid Whistler member, 1.3 metres thick in the more rtoltherly bed assigned to the Ross Creek Formation contains a few section (Figure 45) is not present in the section a kilometre phosphatenodulesas well asdisseminatedphosphatepellets to the south (Figure 46). Here several phosphate bearing cement. Some of the brachiopod shells within the co- and beds are present hut their phosphate content is lower. quinoid bed have been phosphatized. A single sample from this bed returned a grade of 0.9% PzOsover 0.9 metre.Float Phosphorite in the more northerly of the two sections containing phosphate nodules suggests that better grade is composed of dispersed to semicompact brown :o black, phosphate may be present in the area. fine ovoid pellets and a few coarse pellets. The pel!ets, 0.05 to 0.5 millimetre in diameter, occur in a dominantly calcite TODHUNTER (28) NTS: 825/2W matrix with a grain size of 0.1 to 0.3 millimetn:. Minor MINFILE. 082JSEO18 quartz, clay and dolomite are also present in the mitrix and Lat: SO"O7'00" Long: 114°45'30" fluorite is abundant locally. Approximately 10 to I?;%ofthe pellets are nucleated or encased, with the cores i:enerally A small outcropof Permian strata occurs along a log- composed of carbonate, or rarely quartz. __ ging road north of Todhunter Creek (Figure 14). A chert- UIlrr, Mr my_* e, tha"'k0, 0mli.a io P*O, es I-i U. V. ", b, <,0s w" bearing conglomerate 1 to 1.5 metres thick contains black phosphate pebbles. A sample of the conglomerate assayed 2.1% P205. These strata are believed to be correlate with the Per- mian section that extends from Crowsnest Pass to Banff. They underlie Triassic rocks although at this locality the contact was not observed.

ALEXANDER CREEK NORTH (29) NTS: 82G/IOW MINFILE: 082GNE027 Lat: 49"Sl'Oo" Long: 114"47'00"

Wophosphorite occurrences are exposed in roadcuts near the headwaters of Alexander Creek (Figure 14). This phosphorite, which has a minimum thickness of 30 centimetres, occurs at the base of the Fernie Formation. It overlies siltstone of the Sulphur Mountain Formation. A sample across 30 centimetres returned an analysis of 29.4% PzOs. These beds are also enriched in barite, containing in excess of 1.6% barium. Lanthanum, uranium and cerium analyses are 472,293 and 55 ppm. Similar, but slightly lower values for these metals were obtained at the Crow deposit.

PHOSPHATE LOCALITIES IN NORTHEASTERN BRITISH COLUMBIA Phosphatic shale in northeastern British Columbia range in age from Upper Cambrian to Jurassic (see Chapter 3). Thirteen occurrences aredescribed in the following section; numbers in parentheses refer to numbered localities on 1 Pbiohrtb...... P _" Figures 13, 16, 17, 18, 19 and 20, in pocket). Figure 45. Section 87-6, Meosin Mountain north.

Bulletin 98 61 British Columbia -

The coarse pellets are 1 to 2 millimetres in size and contain veryfine grained quartz and some finer pelletal :na- terial. Some carbonate is also present. In the southern section (Photo 27) dispersed pellets are present in a bioclastic limestone unit. The pellets are dark brown to black and structureless; a few have a quartz nucleus. WAPITI LAKE (32) NTS: 931l7>10 MINF'ILE 0931022 Lat: 5P30'00" Long: 120"40'00"

Claims in the Wapiti Lake area were staked by ILso Resources Canada Limited in1979 and were the subject of an intensive exploration program, consisting of geo1og:ical mapping, trenching and diamond drilling, complete3 in 1980 (Heffernan, 1980). South of Wapiti Lake (Figure 16) the phosphate-tear- ing Triassic sequence has been folded into a series northwest-trending broad synclines and tight anticlines (Fizure 47, Photo 28), modified by thrust faulting. The phosphorite bed lies at the base of the Whistler member of the Suhlhur Mountain Formation. It varies in thickness from 0.8 to 3.2 metres with assays varying from 11.9 to 23.7% PzOs and averages 19.7% over 1.O metre (Heffeman, 1980; A. Legun, persod communication, 1987; this study).On theeastlimb of the Wapiti syncline the phosphorite outcrops on s. dip slope, offeringthe potentia1 for open-pit mining with a very low stripping ratio. The base of the phosphorite br:d is marked by a thin phosphatic conglomerate that varim in thickness from 5 to 20 centimetres. In this area the rhos- phate has a high carbonate content as reflected by the CaO: P205 ratios. In places the MgO content and Corg contents are high (Appendices 12 and 13). The average conter t for lanthanum, cerium and ultrium are low compared to ethos- phate in theFernie Formation. Under the microscope the phosphorite is seen lo be Figure 46. Section 87-7, Meosin Mountain south. comprised of dispersed to compact pellets. The pellets are generally brown to dark brown with grainsize ranging from

Photo 27. Stratigraphic section through Vega-Phroso (VP), Whistler(W) and Llama (L) members of the Sulphur Mountain formation south of Meosin Mountain.

62 Geological Survey ?:ranch Ministry of Employment and Illvestment

m- 2 Diornond drill hole ...... 0 Sample location 1985 85-21-1 (A. Legun)...... x sornp1e IoCOtion 1987 5887-12 ...... 5 Syncline ...... 4 Anticline ...... 4- Trend Of fold oxis...... Trench ...... H Thrust fault ......

Figure 47. Geology of the Wapiti Lake area (mcdifed from Heffernan,19080; Legun and Elkins, 1986).

B~dletin98 63 Photo 28. Folded Mississippian (MR), Permian (P) and Triassic Vega-Phroso (VP) and Whistler (W) member strata in the Wapiti Lake area.

0.05 to 0.30 millimetre, although larger nodules are occa- oolites. Pellets are brown to dark brown, generally ovoid, sionally present. The matrix is composed of variable and 0.1 to 0.3 millimetre in diameter. The matrix which is amounts of quartz and calcite with minor dolomite and clay. composed of quartz with minor calcite, dolomite, feldspar It is generally finer grained than the pellets. Some 5 to 15% and illite is finergrained than the pellets. Rare nodule; and of the pellets are oolitic, some with alternating IayeIs of car- compound pellets are also present. Nodules contain both bonate and phosphate; 5 to 60% are eithernucleated or en- oellets and inclusions of auartz. Two samnles from this lo- cased (Photo 11). Manyof the pellets have multiple nucleii; the nucleii may be either quartz orcarbonate grains. Many of the pellets have an irregular carbonate core suggesting replacement of carbonate by phosphate. Fluorite is locally abundant in the matrix. Also present is the rare compound pellet. Some phosphate is also present as cement or as phosphatized bioclastic debris, generally Lingula shells. In addition to the phosphorite bed at the base of the Whistler member, a sandstone bed containing abundant phosphate nodules occurs atthe top of thePermian Mowitch Formation. This sandstone bed is 1 metre thick andcontains 40 to 60% nodules by volume (Photo 29). A cream coloured chert bed 1 to 2 metres thick underlies the sandstone. A sample from the phosphate-bearing sandstone returned a grade of 15.94% PzOs.

MOUNT PALSSON (32) NTS: 93P/4W MINF'ILE 093P022 Lat: 55"05'55" Long: 121"47'20"

At Mount Palsson, immediately south of the Sukunka River (Figure 16) phosphorite is present in felsenmeer near the base of the Whistler member of the Sulphur Mountain Formation. The amount of material present suggests that the phosphorite occurs in a bed that isapproximately 1 metre or less thick. Host lithologies are fineargillaceous and calcareous siltstones. In thin section the phosphorite is seen to be comprised the Permian Mowitch Formation, Wapiti Lake area. of semicompact to compact fluorapatite pellets with a few Minisfry of Employment and hesfment cality averaged 26.4% PzOs, 566 ppm vanadium, 44 ppm In thin section the phosphorite is seen to consist of lanthanum, 42 ppm cerium and 227 ppmyttrium. ovoid pellets in a fine-grained dolomite, quartz anc clay matrix (Photo 30). Some chert is also present. Pellets are suban- BAKERCREEK(33) PITS: 930/1 gular to rounded, dark brown to black and vary from 0.10 MINFILE 0930038 to 0.30 millimetre in diameter. Approximately 5% of the Lat: 55"09'10" Long: 122"06'45" Long: 55"09'10" Lat: pellets are nucleated with either quartz or carbonate grains. Texturally the pellets vary from dispersedto compact. This poorly exposed occurrenceis located north of the Sukunka River (Figure 17) 5 kilometres northwest of the MOUNT LUDINGTON (35) NTS: 98B/6 headwaters of Baker Creek. Here a sandstone bed 1 metre MINFILE 094B029 thick contains 20 to 30% phosphate nodules. It overlies a Lat: 56"27'50" Long: 1:.3"14'30" chert bed near the top of the Permian Mowitch Formation. A sample from this locality contained 11.66% PzOs. The presence of phosphate bearingstrata in the Mount Ludington area south of the Graham River(Figurt: 18) was LEMORAY (34) N2S: 93011 0 first reported by Gibson (1972) in a stratigraphic section MINFILE 0930011 measured at this locality. Phosphate occurs over a strati- Lat: 55"31'20" Long: 122"32'30" graphic interval of 150 metres in the Middle Triassic Toad Formation (Figure 48)as nodules, phosphate-cemmted silt- A sequence of Triassic strata outcrop north of the Pine stone, phosphate lenticles and phosphatic fossil debris in- Pass Highway near Lemoray (Figure 17). These rocks are cluding rare phosphatized fish skeletons. The host rocksare believed to belong to the Toad Formation and the Charlie dark grey to black carbonaceous and calcareous siltstones Lake Formation. The sequence has been foldedinto a series and shales. There is a marked change to lighter coloured of anticlines and synclines and is overlain by shales of the rocks at the top of the phosphate interval (Photo 31). 'The Jurassic Femie Formation. lower part of the phosphatic sequenceis marked b) the presence of large calcareous concretions. The Toad Formation consists of fine siltstone, weakly calcareous siltstone, silty limestone and minor sandstone. Phosphate nodules are black, ovoid to spherical, some- Phosphatic beds occur sporadically throughout the section times irregular, 1 to 3 centimetres in diameter and comprise and include a phosphorite bed 1 to 2 centimetres thick. The 5 to 20% of the rock by volume. Theystand out ir relief on phosphorite is overlain by a thin crossbedded siltstone in weathered surfaces. Individual nodular units are generally which bedding is marked by black phosphatic laminae. 1 to 2 metres thick and rarely as much as 10 metrcs thick. ~~~~~~ ~ ~. LAURlER PASS NORTH (36) NTS: 94B/13 MINFILE 094B030 Lat: 56"50'55" Long: I;.3"31'30"

Phosphate occurring in the Toad Formation was reported by Gibson (1972) from a section measured in the 140 headwaters of Calnan Creek. To the south, toward Lanrier Pass (Figure 18) phosphaticstrataareexposed on both limbs of a broad open anticline over a stratigraphic interval of at lie ..... , least 100 metres (Figures 49 and 50). As at Mount Ludington, phosphateis dominar.tly nodular, although phosphatic cementis also be present.Nodular beds are generally 1 to 3 metres thick. The nodules are black in colour, ovoid to spherical and occasionally inegular in shape and rangein sizefrom 1 to 3 centimetres ac:.oss; they may contain multiple quartznucleii, no internal structure or, ri rarely, an ammonite. They are interpreted to have formed diagenetically, probably below the sediment-water interface. Host lithologies consist of shale, carhonaczous and weakly calcareous quartzosesiltstones. Most ofthese rocks are weakly phosphatic. Calcareous concretions (Photo 32) PhOOdk...... P occur in the lowerpart of the phosphatic sequence together .~ with an abundance of phosphaticlenticles. Figure 48. Section SB87-34, Mount Ludington. Photo 30. Photomicrograph (40x) of phosphatic limestone, Lemoray. Phosphate pellets (black)are dispened in a carbonate-rich matrix. Some chert (lower Icft) and quartz are also present.

s*rr+dr d"b> . m,,*#< ......

Figure 50. Section SB87-36(3), Laurier Pass north (measured on west limb of anticline approximately 60 metres upsection from Figure 49. Scction SB87-36, Laurier Pass north. Section SB87-36).

66 Geological Survey Branch Ministry of Employment and .‘nvestment

Photo 31. Section through the Toad Formation (T)and lower portion of the Ludington Formation (LUD). Hatched line marks the change fromweakly Carbonaceous - phosphat sedimentsto more calcareous - nonphosphatic sediments.

Photo 32. Phosphatic nodulesand a solitary calcarcaus concretion in sillstone of the Toad Formation from a locality north of Laurier Pass.

RICHARDSCREEK (37) NTS: 946/12 Lithologies consist of very weaklyphosphatic chert and MINFILE. 094G022 siltstone of the Fantasque Formation. The contact with the Lat: 57”37’30” Long: 123”40’00” overlying Toad Formation is unconformable, the Grayling A thick phosphatic interval is exposed along a south- Formation being absentat this location. Triassic L trata con- flowing tributary of Richards Creek west of Trutch on the sist of carbonaceous and calcareoussiltstones and interbed- Alaska Highway (Figure 18). Phosphate was first reported ded shales. at this location by Pelletier (1964). A section from the top Phosphate-bearing rocks occur overa stratigraphic in- of the Permian Fantasqne Formation to the Upper Triassic terval of 290 metres in the middle Toad Formation instrata is exposed. Figure 51 is a section measured from the top of of Anisian age. Phosphate nodules occur in several beds the Permian to the top of the phosphate-bearing interval. over an interval of 220 metres. Nodules are the dominant .....

Siltstone: argillaceous, darkgrey lo blockweathering and colour; thinbedded: recessive: weakly CorbonOCeoUE; coIcoreous, lloggy weathering; 4ome iominotioo5present ......

Siltstone:grey wealhering: dark grey to block. thin to mediumbedded: reSiEtmt: quartzose. cancretioniry weathering appeoronce = 3.05.83.1822.24.69 SiltEtone: greyweothering: dark grey to black.weakly phosphatic: top 1 m contains phosphatenodule(, Siltstone - rhcle: dork greyweothering: dork grey to block. thin bedded:carbonaceous; recessive Covered intelval Siltstone: dork giey weothering,dark grey to block; thin bedded:weakly CorbonOCeOUs: weokly phmphaiic Siltstone: coIc~reo~s:dork grey weothering; darkgrey to block thin to mediumbedded; resirtont = 4.89,42,1092,71,<7,20

Siltstone: grey wealhering: darkgrey weathering. dark grey to block,thin bedded: very weakly phorpha,ic; resistant Siltntone:dark grey weatheiingi dork grey to block.thin bedded. resistonl: weokly CorbOnmeOuS, quotiiose; phosphatic; few phosphatenodules present Cnvcred...... i"l<,"d Siltstone:dark grey to black thin bedded:moderately resistont: few indistinct phosphatenodules; quariose Coveredinterval Siltstone = 1.94,20,85,51,2,27 Siltstone: dark grey to blockweathering and colour; corbonoceous;medium bedded; phosphotic. relaiivdy resislant Siltstone: dark grey to blackweathering and colo~r:thin bedded:relatively reslstont, ledgeformer; wertly = 3.00.18.119,49,<7.36 phosphatic: few phosphate nodules (less than 5% byvolume) =0.59.16.115.29.<7.117

z Siltrtone - shale: doh grey weothering: darkgrey to block;medium bedded: few coIcoreous concretioie 0 near top: wokiy eotbonaceom % I - 2.76 20 134 637 52 a = 2.65:15:133:61:18.45 Siltstone:grey to darkgrey weathering and colour: phorphote nodules and c10sto present Coveredinterval e Silt~tone- shaleinterbedded: grey lo brownishgrey weothering; dock grey to block thin bedded,Ilagqy; D 4 few very thin, weoklyphosphatic beds. c~lcoreo~~,weakly CwbonoCeOus Siltstone: orgillaceo~s:dah grey to block weotheringand COIOY~.recessive, thin bedded. weakly e = 0.68,18,748.55,16,70 CorbmOCeoUE;phosphatic lenses present Siltstone:grey to darkgrey weathering and eolour; thin beddedweokiy phosphatic Siltstone:omnge weathering, grey to dah grey; thin to mediumbedded. phosphate lenses present Siltstone - shoie: dah gre rece~sive = 1.63,12,767,48,18,84 Siltstone: brownish orange greyweqlhering; grey. lIag2r; cpntainsthin phosphatic lenses Siltstone: pale oronge to grey weathenna; dark 9rey to ack. flaoav. fore DhosDhatenodules ~ ~...... Siltstone:grey to orange weathering; grey to dark grey: thinbedded, flaggy, cuIc0reous weoklycaibontlceous

Covered interw

Siltstone: grey to dockgrey weathering; doh grey to black:thin bedded. floggy. weokly phorphotic; rei:essive

Siltstone:grey to dark gery weathering;dork grey to black,thin beddee. flaggy, recerrlve; thin bard conglomerate

Chert:weokly phorphotic. rerirtant Phosphate nodules ...... *- Phosphate len~es...... 0 Calcareous concretionr ...... - Phorphatic ...... P

Figure 51. Section SB87-37, Richards Creek.

68 Geological Survey Branch form of phosphate comprising 5 to 40% of beds in which 5.56% P205. Bedding strikes northwesterly with moderate they occur. Nodules are typically black, ovoid to spherical dips to the southwest. A second bed, 70 centimelres thick, and vary in diameter from 1 to 3 centimetres. Thin beds of 55 metres higher in the section contains 10.12% 1’205. pelletal phosphate are alsopresent in the middle portion of Phosphate is present as disseminated pellets .md a few the phosphatic sequence. Calcareous concretionssimilar to black nodules. Pellets are 0.1 millimetre in diameter con- those at Mount Lndington and Laurier Pass Northare pre- trasting with a finer grained matrix. They may constitute as sent at approximately the same stratigraphic position. much as 40% of the rock but generally constitute less than 20% of the volume. TETSA RIVER -ALASKAHIGHWAY (338-40) NTS: 94H9 SUMMIT LAKE (41) NTS .94K/lO MINFILE: 094K080,081,082,083 MINFILE 094K084 Lat: 58”40’00”Lat: Long:124”17’30”to 124°26‘30” Lat: 5S040’00“ Long: 121°36‘00”

Several phosphate occurrences are present in outcrops Shale and chert of the Permian Kindle Formation are of Toad Formation in a folded sequence of Permianto Upper exposed along the Alaska Highway approximately 2 kilo- Triassic strata exposed along the Alaska Highway north of metres east of Summit Lake (Figure 20). ‘Withi1this se- the Tetsa River (Figure 20). quence and overlying the chert is a 5-metre interval Both pelletal and nodular phosphate occur in carbona- containing phosphatic laminations and lenses. The lamina- C~OUSsiltstone, shale and limestone of middleTriassic age. tions are distinguished only bytheir black colouril contrast At the most easterly of these occurrences (Locality 38) a to the dark grey of the shale. Overlying the phosphatic se- phosphorite bed 15 to 20 centimetres thick is present in a quence are brownish to brownish grey siltstones. b. sample sequence of dark grey carbonaceoussiltstone and limestone. across 2.5 metres at this locality averaged 3.60% P205. This sequence is 3.3 metresthick and averages 4.30% P205. The phosphorite bed is pelletal with the pellets varying in GREY PEAK (42) NTS., 94F/14 size from 0.05 to 0.15 millimetre. The majority contain MINFILE 094K019 quartz nncleii or an occasional carbonatenucleus. The ma- Lat: 57O48’00” Long: 1;.5°12‘00” trix consists of quartz with minor calcite and very minor feldspar. Also present are rare phosphatized shell fragments Phosphate was first recognized in the Grey Peak area or nodules and some phosphate cement. There are a few in the headwaters of the Kwadacha River (Figwe 13) by nodules in the siltstone. Bedding at this locality is flat to very Cecile and Norford (1979) while conducting strrtigraphic gently dipping to the west; beds vary in thickuess from 50 studies of the Upper Cambrian-Lower Ordoviciar. Kechika to 100 centimetres. Formation. They observedthat several thin phosphate hori- Two kilometres to the west (Locality 39) another phos- zons were present inthe upper 100 metres of the formation. phorite bed, 15 centimetres thick, is exposed in a sequence Phosphate also occurs at several horizons in the lower of siltstone and dolomitic siltstone within the Toad Forma- banded limestoneunit; they describethese lower F hosphate tion. It consists of 15 to 25% dispersed pellets in a matrix of occurrences as “sea-floor pavements or lag depos.ts”. quartz and minor carbonate. Pellets are subangular to Thin phosphaticbedsoccur at five horizonsin theupper rounded and 0.2 to 0.3 millimetre in diameter. The majority 100 metres of the nodular limestone unit of the Kechika contain quartz core oroccasionally carbonate core; a few a a Formation. Phosphate is present as microcrystalline coat- have both quartz and carbonate nucleii. Some pellets have ings, 1 to 10 millimetres thick, around limestone nodules, feathered contacts withinternal carbonategrains suggesting and as phosphatized fossil debris (trilobite) in betls 5 to 50 that replacement of carbonate by phosphate has taken place.centimetres thick. Some pelletal and oolitic phosphate is Within the phosphorite bed there is a layer 5 centimetres also present. These phosphatic beds are easily recognized thick in whichthe volume of pellets increases to 50 or 60%. by their blue weatheringsurfaces and black colourcontrast- Immediately to the west of this exposure, phosphate is ing withthe pale greyof the host limestone (Photo33). Also present as disseminated pellets and nodules in outcrops of present, hut not obvious,are thin phosphaticcoatiqs, 1 mil- dark grey siltstone. Nodules and pellets are 0.5 to 1.O centi- limetre or less thick, surrounding limestone nodules in beds metre in diameter and black colour,in in contrast to the dark 2 or more metres thick. grey colour of the siltstone. Some of the siltstone is very Cecile and Norford (1979) interpret the Kechika F’or- weakly phosphatic. Dessication cracks andripple marks are mation in this area to represent an outer-shelf environment. seen at this locality but not elsewhere in area.the Deposition Phosphate deposition was shallow enough thatperiodic fur- of the phosphate appears to have taken place in extremely bulence caused some phoscrete beds to be ‘broken up and shallow water during which there may have been short pe- redeposited, although the transport distance ]nay have been riods of subaerial exposure. very short. The most westerly of the phosphate Occurrences outcrop at Kilometre 607.5 on the Alaska Highway (Locality 40). An interval of phosphatic siltstone and limestone 2.5 CARBONATITES metres thick occurs in a sequence of dark greyto black ar- Carbonatites andrelated alkaline intrusives arc the sec- gillaceous limestone and calcareous shale and averages ond most important source of phosphate, accountingfor ap-

BuNefin 98 69 .. . Grey Peak area.

~ proximately 20% of world reserves. Resources of igneous 1 phosphate rock have been estimated at 9 billion tonncs av- S edimentary IgneousSedimentary eraging 4% PzOs or more (Notholt and Highley, 1986). 401 These deposits are expected to become more attractive as potential sources of phosphate, particularly in areas where sedimentary phosphate deposits are absent or ofpoorqual- ity. Beneficiation technology is such that very low grade deposits can yield concentrates of very high grade.A comparison of marketable products from sedimentary and igneous phosphate deposits is shown in Figure 52. Igneous phosphate deposits are generally associated with nepheline syenites stocks or carbonatite comp.exes; phosphate is normally present as apatite. Production of phosphate from igneous rocks is limited to eight countries. Canada docs not produce any igleous phosphate but does have substantial resources in Ortario; MarketableProducts 40 recent work indicates that significant resources of igleous phosphate may be present in BritishColumbia. Emigh (1983) suggests that deposits containing 15% recoverable apatite (6% PzOs) may be of economic ir terest provided there are adequate reserves and that location and operating costs are favorable. Phosphate-bearing carbna- P tites have been recognized at several localities in E~ritish 10 Columbia (Figure 53). At thepresent time none contain sufficient phosphate to be considered potentially economic 1 based entirely on this single commodity. It is feasible, however, that phosphate could be produced as a byprod Ict in recovery of rare-earth elements.

Figure 52. Comparative grades of sedimentary and igneous phosphate ores and marketable products (from Notholt and Highley, 1986).

__ 70 Geological Survey Ikanch I LOCAllTIES

Figure 53. Map showing locationsof phosphate-bearing carbonatites (modifedfrom Pell, 1987).

ALEY NTS: 94B15 MINFILE 094B027 L at: 56"27'00" Lat: Long: 123"44'50" Figure 54. Geological map of the Aley carbonatite and sample locations (from Madcr, 1987). The Aley carbonatite complex (Figure 54) is described as an oval body, approximately 3 to 3.5kilometres in diame- (l985,1987)andAaquist(1981)andonah1iefexamination ter, consisting of a dolomite-calcite carbonatite core with an by the author. outer ring of metasomatically altered syenite (Mader, 1987; Pell, 1987). Apatite is present as fine-grained crystals Two types of carbonatite are present at the Vcrity local- (Photo 34), averaging approximately 0.2 millimetre in ity: a white-weathering sovite containing predominantly length, and aggregates in bothphases of the core but is more calcite (60 to 85%), olivine (3 to 20%) and apatite (2 to 20%) abundant in the calcite-carhonatite phase. K.R. Pride (oral and a buff-weathering dolomitic carbonarite (r,ruhaugite) communication, 1987) suggests that the average grade of containing amphibole (5 to 15%) and apatite (2 to :IO%). The apatite occurs as subrounded grains 1 to 4 millimetres in the carbonatite is approximately 5% PzOs representing approximately 10% apatite. Chemical analyses by the author diameter. Grades of 2 to 5% Pzo5 have been recorded by and Pel1 (1987) indicate phosphate values of 1.44 to 6.07% Anschutz (Canada) Mining Limited (Aaquist, 1981). Sam- pling by the author and Pel1 (1987) obtained pho:;phate val- p205. ues ranging from 0.21 to 2.52% Pzo5. Sample;; fronr the VERITY NTS:83Dl6 Paradise and Howard Creek carbonatites to the. east contained 4.12 and 5.45% Pzo5 respectively. The resource po- MINFILE 083D005 tential for the Verity carbonatite is only a few milion tomes. Lat: 52O23'55" Long: 119"09'25" REN (RutchfordCreek) NTS: 8ZM17 The Verity carbonatite is one of several carhonatites MINFILE 082M199 exposed east of the Yellowhead Highway inthe Blue River Lat: 51"21'30" Long: 118"44'30" area (Figure 55). Unlike the Aley complex the Verity carhonatite is a tabular body that has undergone intense structural deformation (J. Pell, oral communication, 1987). The Ren carbonatite outcrops on the slopes south of Descriptions of this locality is based on the work of Pell Ratchford Creek in the core of the Mount Grace syncline

Bulletin 98 71 Photo 34. Photomicrograph under cross-nicols (40x1of subrounded apatite (Ap) crystals disseminated in a carbonate matrix, Alcy carhonatitc.

between the Seymour Arm of Shuswap Lake and the ~ZO- lumbia River. It is a concordant unit 3 kilometres long and 20 to 300 metres thick. The following description is summarized from Pilcher (1983), Pell (1987) and Hoy (1987). The Ren carbonatite is a massive to well-layered, orange- brown weathering body consisting of 60 to 80% ,:a]- LEMPRIERE cite, IO to 30% apatite and accessory biotite, amphibde, pyroxene and sphene. Minor amounts of pyrhotite, magnet- 1 ,PARADISE LAKE ite, pyrite, ilmenite, sphalerite, chalcopyrite, pyrochlon:(?) MOUNT LEMPPIiERE A3450m and monazite(?) are also present. Mafic feniteoccurs almg HOWARD CREEK' the margin and within the carbonatite. It is enriched in Lght PYRAMID CREEK rare-earth elements and lanthanum. Grab samples collected \b by Hoy (1987) across a 30-metre section of the cslrbonatite averaged 3.39%P205. The resource potential of this deposit is in the order of several million tonnes of very low glade material.

THREE VALLEY GAP NTS: 82Ll16 MINFILE 082LNE44 Lat: 50O57'30" Long: 11 8"29 00"

Discontinuouslenses ofcarbonatite, parallel to bedding in pelitic sedimentary rocks outcrop along the Victor Lake logging road whichjoins tbeTrans-Canada Highway from the south, approximately 3 kilometres east of Three Valley Gap (Pell, 1987). The carbonatites are composed of 45 to U 50% calcite, 5 to 20% biotite, 5 to 15% apatite, up to ;O% BLUE RIVER perthite, 5 to 30% hornblende and 1 to 10% augite. Trxces of sphene are also present. Rare-earth element content are Corbonotite rites 0s noma6 ...... rn low. Three samples collected by Pel1 (1987) averaged234% Pigure 55. Blue River area. Map showing carbonatiteand P205. The resource potential for phosphate at this location sample locations (from Pell,1985). is very limited.

__ 72 Geological Survey Brznch Ministry of Emplgment and Irvestment

UPPER ORDOVICIAN AND DEVONIAN TO MISSISSIPPIAN ORYOUNGER Black pelite unit

LOWER CAMBRIAN Mural Formation

HADRYNIAN AND/ORCAMBRIAN Midas Formation

HADRYNIAN (WLNDERMERE) Yankee Belle Formation

SYMBOLS Fault ...... Thrust fault ...... - Sample location...... x S887-29 Phosphate onalyses ......

~~ ~~~~ ~~ ~~ Figure 56. Geology and phosphate occuncnces in the Cariboo Lake - Spcctaclc Lake area(9N14 and 93W3)

Bulletin 98 73 MISCELLANEOUS PHOSPHATE GRANDUC TAILINGS OCCURRENCES Grove (1986) reports that apatite up to 25%and aver- Several other phosphate occurrences not covered ear- aging 10% occurs in calcsilicate rocks and limesto,nes lier in thisreport, are present throughout British Columbia. within the ore zoneat the former producing Granduc mine. While none of them show significant economic potential Analyses fronisomeofthese rocksreturned vaIuesof2.42% they illustrate a variety of forms in which phosphate may PzOs. Granduc tailings were sampled to determine if tbere occur. had been any upgrading theof phosphate content duringthe concentration process. Results are uniformly low (0.22% QUESNEL AREA PzOs) indicating that no upgrading has taken place andthat Campbell, et al. (1973) recognized the presence of the Granduc tailings have no potential for recovering pbos- phosphate in the Lower Cambrian Midas Formation while phate. mapping in the McBride area. They reported that sandstones, containing up to 25% collophane grains, are present IRON MASK BATHOLITH in the northern Caribou Mountains. These strata extend Steeply dipping tabular magnetite-apatite lodes (hat southward into the Wells - Barkerville area. Also in this vary in thickness from 1 centimetre to 3 metres andcontain- area, marine sediments of the Black Stuart Group, interfn- ing up to 3% PzOs are reported in the Iron Mask Batholith gered with volcaniclastic rocks and pillow basalt of the (Young and Uglow, 1926). The maximum extent of these Waverly Formation are locally phosphatic. This investiga- lodes is 200 metres (Cann and Godwin, 1983). Massive tion concentrated on an area east of Wells and specifically magnetite containing white or pale pink euhedral apatite in the Cunningham Creek area (Figure 56). Analyticresults crystals is present at the Magnet locality. Apatite and zm- are presented in Appendices 17, 18 and 19. phihole crystals frequently occur in layers adjacent to the The Black Stuart Group hasbeen divided into three in- walls of these lodes. formal units (Struik, 1988). The lowermost unit consists of graptolitic shale and is overlain by a chert-carbonate unit. FRANCOISLAKE ASPHALTUM NTS: 93IV4 In the vicinity of Black Stuart Mountain this middle unit is MINFILE 093K056 45 to 90 metres thick (Campbell et al., 1973). The upper Black pelite unit is less than 500 metres thick and consists Lat: 54"04'55" Long:125"45'00" of siliceous shale, phyllite, greywacke and minor limestone and calcareousschists. Present withinthis unit are thin beds A small showing of botryoidal phosphate and asphal- containing disseminated barite and phosphate. Sphalerite is tum occurs 2 miles north of Francois Lake.irregular An win also present locally but isnot directly associated with phos- 10 to 30 centimetres wide outcrops over a strike length of phate. Grades of 3.55 to 8.00%PzOs were obtained over about 30 metres and cuts amygdaloidal and vesicular :In- thicknesses of0.7 and 0.5 metre respectively at two separate desitic flows of Tertiary age. These flows overlie sandstme localities. and shale. The phosphate minerals present have beenidcn- The Black Stuart Groupis interpreted to have beende- tified as collinsite [Ca2(Mg,Fe)(P04)zZH20] and quercy ite posited on a gently undulating unconformable surfacedur- (3CaOPzOsCaOCOzHzOCaF2) (Armstrong, 1949). ing the Orovician (Struik, 1988). Graptolitic shales were Phosphate occurs as nodules, 5 to 20 centimetres in rli- deposited in a quiet stagnant basin whilethe overlying chert- ameter that consist of botryoidal masses of concentric lay- carbonate unit was deposited in shallower water.The upper eringofphosphatewithanoutercoatingofblackasphaltum. Black pelite unit was depositedin a basin that was quiet and Mostofthenodulesencloseanangularfragmentofandesite. restricted with little clastic input.

74 Geological Survey Branch CHAPTER 7 BENEF’ICIATION AND PROCESSING OF PHOSPHATE ROlCM

The purpose of heneficiation is to raise the PzOs level Calcination is required if the organic content is too high as to commercial standards(30 to 37% PzOs) and to reduce the organic matter causes foaming during acidulation. It may proportion of carbonate, iron and alumina oxides, organic also be required to remove excess carbonate. matter and suchtrace elements knownto bepoisons as cad- While the phosphate specifications are designed pri- mium, nickel and selenium. Canadian fertilizer plants are marily for Florida phosphate (Kouloheris, 1977), they also designedforfeedstockcontaining31.1 to33.0%PzOs.Most phosphate rock requires some beneficiation prior to ship- TABLE 12 ment to processing plants. Spica1 specifications for phos- PHOSPHATE SPECIHCATIONS REQUIRED BY phate content and majorimpurities are snmmarizEd in Table FERTILIZER PLANTS (from Kouloheris, 1977) 12. Only under humid andacidic soil conditions phosphate

~~~ rock may befinely round and applieddirectly as fertilizer. _” The first stagein the production of phosphate fertilizer Pz Os content: 27 to 42%. is the conversion of phosphate rockto phosphoric acid. This CaOiPzOs ratio: 1.32 to 1.60. is generally done by either a “dry” or “wet” process. These A1203 + Fez03 + MgOPzOs .I (optimum value). processes are outlined in Figure 57. Most commercial fer- MgO tolerance is approximatly1 .0%, less than 0.8% is lecessary tilizer plants use the wet acidulation method in the initial for the manufactureof triple super phosphate. stage of fertilizer production. In the wet process phosphate SPUMgO ratio : 170 or higher. rock is must commonly treated with sulphuric acid to pro- BPLlAIz03 + Fez03 ratio : > 20. duce phosphoric acid, and gypsumas a waste product. High BPLlCaO ratio > 1.5. calcium and magnesium carbonate contents in the phos- Iron and aluminum as per cent Fez03 and A1203 shou .d be less phate rock are undesirable in the processing of phosphate than 5%. rock as are high iron and aluminum contents. High carbon- BPL =Bone phosphate of lime(2.1852 x per cent 1’20s).

sulphuric (most common treatment)

concentroted super phosphate super concentroted normol super phosphate

ummonium furtherpurification fertilisers phosphatephosphate fertilisers for ierti1isers chemical productionchemical ierti1isers

nitricocid - nitricphosphate elemental phosphorus is fertilisers producedto make very pure I phosphoricocid. “Sed to produce /I’ 3 Electric F~rnnce chemicalsand. when further processed, to make food- hydrochloricacid - phosphoric gradephosphoric acid acid (very limited we) (From RUSSBII,_- 1987) Figure 57. The different methodsof treating phosphate rock.

Bulletin 98 75 apply to other deposits (Table 12). In general, if the Cao/P205 ratio exceeds 1.6l:l sulphu- Rock with a high magnesia and alumina content pro- ric acid consumption by the calcite is too high for an eco- duces acid of high surface tension and viscosity. Iron and nomically viable process. The effects of the various alumina are believed to influence the development of gyp- impurities are summarized in Table 13. sum whichin turn affects the recovery ofPzOs. Slimes, pri- All phosphorite deposits in British Columbia will re- marily colloidal clay material, tend to adhere to phosphate quire beneficiation prior to their use in fertilizer plants. ?he grains and also to float with the concentrate during the flo- amount of beneficiation required is dependent upon 'the tation process; clay coatings on phosphate particles impede amount of ganguepresent; the higher the phosphate content the attack of sulphuric acid. Desliming is therefore used to the easier it shouldbe to effect phosphate liberation. Factors remove clay fromthe phosphate rock. affecting the processing, especially the grinding and flotation of phosphate rock include phosphatedispersion, grain

TABLE 13 EFFECTS OF IMPURITIES IN THE MANUFACTURE OF FILTER-GRADE WET-PROCESS PHOSPHORIC ACID

~~ PRACTICAL LEVELS FOUND IN DESIRABLE UNDESIRABLE AMOUNT OF IMPURITY IMPU RITY FEEDSTOCKIMPURITY PROPERTIES PROPERTIES PASSING INTO ACID "

Aluminnm 0.2-3% A120i Reduces corrosion by Forms complex phosphates which impair 70-90% fluoride ion filtration, increase acid viscocity and precipitate. Iron 0.1-2% FCiO3 May be recoverable as Forms complex phosphates. Strong 60.90% iron oxide influcnce an acid viscosity;farm sludge.

Magnesium0.2-0.6% MgO May have Farms eomplcx phosphates and nutrient value fluosilicatcs; impcdcs tiltration; affccts downstream product quality. Fluorine 2.4% Fluorine Can bc rcactcd and Likratcd partly as IIF: part held by filter; 25-75% recovered as by-product pan may cantributc to sludgc fonnation. More iluorinc gcnerated during concentration. Ifl12SiF6 fonncd by rcaction with Si02 may modify crystal formation.

Silica 1.10% Si02 To convertHF to less In high proportions E~USCSerosion 5.40% aggrcssivc fluasilicic acid problems (li2SiF6) Strontium and 0-3.0 SKI Inhibits recrystallionofhemihydrate La. lanthanides(for example) gypsum. Insoluble compounds formed in 40 wt-% P2Os acid. Chlorine 0-0.05% Above 0.03% can give~everc corrosion 100% with wrong materials.

Carbonate 0.7-8.0% Incrcascs sulphuric acid consumption n.a. Organics 0.1-1.5%C Stabilize foams during acidulation. Impair 15-70% filtration by "blinding" cloth. Disealour product acid. Cadmium 0.8-255 ppm Significant proportion passes through into 70% acid and downstrcam products. Toxic metal. Uranium35-400ppm U308 Is recoverable and may be soldas by- 7540% product

" Source: Phosphorus & Potassium No. 146 (From Russell, 1987).

__ 76 Geological Survey Branch size of gangue minerals, pellet size, relative hardness of the Sulphur Mountain Formation. Textural and mineralogical minerals present, proportion of gangue material present in summaries for phosphate deposits in British Columbia are the pellets, strength of intergranular bonding agents and the presented in Tables 14, 15, 16 and 17. nature of gangue replacement of phosphate (Mabie and Phosphoritedepositsin the Whistlermemberof theSul- Hess, 1964). phur Mountain Formation tend to be moderal.ely tcs poorly In theirpetrographicstudy of thePhosphoriaFormation sorted and contain numerous nucleated or encased pellets Mabie and Hessattempted to relate petrography and miner- whereas phosphorite in the Fernie Formation tencls to be alogy to the metallurgical characteristics of the phosphate well sorted with only a few encased or nucleated pellets. rock. They suggested that petrographic characteristics can Both exhibit pellet sizes generally larger than the matrix. beusedtopredictthebehaviorofphosphaterockinroasting, Whistler member phosphorites will probably requin: a finer grinding, sizing, desliming and flotation processes. grind to liberate the nucleii present in the pellets. :%ere is Phosphate rock with a high carbonate or organic con- no extensive replacement of pellets in either of there phos- tent may require roasting or calcining at temperatures vary- phorites. Oolites present in the Whistler member may pose ing from 500 to 900°C. Differences in size between gangue grinding problems as they contain alternate carbonate and and phosphate pellets will affect the grinding of phosphate phosphate layers. Pellets will break along the oolitt: layers rock. In most British Columbia deposits the phosphate pel- and carbonate may be floated away along with the elclosed lets are coarser than the gangue minerals. Coarse grinding phosphate if the grind is not fine enough. will tend to concentrate the phosphate particles in the Calcination will be required where the carbonate con- coarser fractions. In arenaceous ore the phosphate will tend tent is high. The Whistler member is invariably calcareous, to be concentrated in the finer fractionsbecause the softer especially in the Wapiti Lake area where CaOR205 ratio phosphate will be more easily broken up than the harder exceeds 2/1 in the majority of samples. Calcination fol- quartz. Mabie and Hess suggest that the effectiveness of lowed by slaking will probably be required to remwe the concentration in the coarser fraction isdependent upon the carbonate. Locally, where dolomite is present somt: selec- tendency of the gangue to break down into fines and be freed live leaching may be required. The carbonate corttent of from the fluorapatite. Clay and sericite can easily be sepa- Fernie phosphorite is zoned (see Chapter 3); calcining will rated by mechanical agitation whereas liberation from be necessary in high-carbonate areas. It is also antiipated quartzose material is more difficult. that desliming will be required to remove excess cla:r mate- Pellet dispersion affects both the grade of the phosphate rial from Fernie phosphate. rock and the ease with which phosphate can be liberated In 1974 Energy, Mines and Resources Canada carried from the gangue. In a study of flotation of phosphorite from out a beneficiation test on a sample of Fernie phosphate a deposit in Idaho, pellet size and initial phosphate content from the Lodgepole Creek area south of Fernie. The sample were the principle factors controlling concentrate grade and was from a surfacetrench and averaged 10 to I1 % 1'205. It recovery (Town, 1967). Liberation of dispersed pellets re- also contained approximately 20 % calcite with minor quires more grinding and therefore increases the proportion amounts of quartz, feldspar and traces of mica anti mafic ofphosphate recovered in finer fractions. minerals (Hartman and Wyman, 1974). The resu1.s indi- The amount of liberation of phosphate particles from cated recovery of 31.5 % with a maximum grade of 28.5 % the gangue will effect the flotation process. Excessive grind- PzOs by attrition methods andrecovery of 49 %with ;I maxi- ingincreases the productionof s1imes.hdeposits with well- mum grade of 28.5 % P20s by hot conditioning and flotation compacted pellets, grinding to sizes coarser than the pellet with soda ash and oleic acid. size may be suitable for effective flotationbut nucleated or Hartman and Wyman also report: "The highes: grade encased pellets require grinding fine enough to liberate product was achieved using a chemical treatment: attrition these very fine particles. and ultrasonics. This grade occurred in the65 and lOI)-mesh Mabie and Hess point out that replacement of pellets (0.25 to 0.15 millimetre) fractions. Flotation result!; using hot conditioning with soda ash andoleic acid show the im- by gangue (clay, sericite, and carbonate) gives rise to textures that may affect the efficient flotation of the phosphate portance of screening and grinding to free and clean sur- rock. Replacement usually follows pelletboundariesand in- faces. Results are even better when ultrasonics are included. ternal structures that are lines of weakness along which the The approach to beneficiation using hot conditioning, al- material will break upongrinding. As a result, the fluorapa- though a costly step, appears promising. The results suggest tite pelletswill break down to particles that are coated with that concentration by attrition and/or other mec1.anical gangue and therefore will behave as gangue during flota- means followed by heavy liquid separation should t.e con- tion. sidered". This investigation was notcarried through t>com- pletion because of the low grade of the sample. To the author's knowledge, Cominco Ltd. is the only BENEFICIATION OF BRITISH company that has completed beneficiation tests on phos- COLUMBIA PHOSPHORITE ROCK phate rock from southeastern British Columbia. Ccminco Although the criteria developed by Mabie and Hess has tested samples from the Lizard, Crow and Mount Lyne (1964) relate to the Phosphoria Formation they may also be deposits. This work, now more than ten years old, was not applied to British Columbia phosphate deposits, especially totally satisfactory as the basal phosphate of the Fernie For- those in the FernieFormation and Whistler member of the mation has a strong hydrophyllic character and cannot be

Bulletin 98 77 TABLE 14 TEXTURAL AND COMPOSITIONAL FEATURES OF ISHBEL GROUP PHOSPHATES

Sample PellevNoduleNature of PhosphateGangue Size GanguePhosphate Organic Ira" CarbonateCompasitianGrade Number Size Phosphate Size Number Dispersion (mm) ReplacementContentContent Content (%PZOS) (mm)

SBB86-81 2-5 Mainly nodules Disoersed 0.05 Mainly quartz with Slightly Phosphatic, 14.63 with some intra some cherty carbon quartzose clasts; nodules sponge spicules aceous or siltstone contain quartz bituminous nucleii

SBB86-57 0.1-0.5 Ovoid pellets Semi-cornpact 0. I Mainly tine Minor Slightly Calcareous Quartzitic 14.71 with 5% nucleated to dispersed grained calcite carbonate carbon- phosphorite and 5% encased; with minorclay aceous or rare 0olite;rare bituminous :! radial structure

SBB86-58 0.3-0.5 Ovoid pellets Semi-compact 0.1 Fine-grained Slightly Quatzitic 24.59 with 5% nucleated to dispersed quartz carbon- phosphorite me oolite, aceous or intraclasts or bituminous nodules

SBB86-71 0.8 to 0.78 Nodular with few Dispersed 0.1 Mainly quartz Slightly Phosphatic 14.4 I ovoid pellets and carbon- quartzose phosphatized aceous or siltstone biaelastic bituminous material

SBB86-79(1) 0.1 Ovoid pellets Dispersed 0. I Mainly clay with - Slightly Quartzitic 24.59 with less than some quanzand Carbo" phosphorite I% containing very minor dolomite aceous or tlUCleii; bituminous phosphate Cement

SBB86-80 0.05-0.2 Ovaid pellets Semi-comDact0.08-0.2 Mainly calcite Minor Slightly CalcareousPhosphatic 5.93 with 75% nucleated with very minor replament carban- limestone less than 5% quartz by carbonate aceous or oolites; few bihlminous radial structures TEXTURAL AND COMPOSITIONAL FEATURES OF THE WHISTLER MEMBER PHOSPHATES

Sample Pellet Size Nature of Phosphate NatureofSampleSizePellet Gangue Size Gangue Phosphate Organic Iron CarbonateComposition Grade (mm) PhosphateNumber (mm) Dispersion (mm) Content Replacement Content Cedent (% PZOS)

SB87-6 0.05-1.00 Ovoid pellets Semicompact 0.10-0.30Dominantlycalcite Minor Highly - 23.64PhosphoriteCalcareous with 10.15% towith dispersed minarquam, carbonate carbonaceous nucleated or quart, clay and very or encased;rare and dolomite minor clay bituminous nodule

SB87-I I 0.05-0.25Ovoid pellets Dispersedto 0.05-0.10 Quem with lesser Moderately - Calcarious Phosphorite26.39 with 25% nuc- semi-compsct cz!cite;miiio: Ca&Cbcr.XeCLLS leated; 5.10% dolomite, feldspar or are oolitic and clay bituminous

SB87-120.10-0.25 Ovoid pellets Semisompact 0.05-0.10Calcite with lesser Minor to Moderately - Phosphorite28.3Calcareous with 30.40% quartz and trace moderate carbonaceous nucleated or and carbonate dolomite or encased;l0-15% and bituminous are oo1itic;some le~serclay nodules and clasts and phosphatized bioclastic debrjs

SB87-150.10-0.30 Ovoid pellets Compact0.05-0.10to Quam withcalcite, Slightly - Phosphorite28.02Weakly with 10.15% semisompact minor dolomite and carbonaceous Calcareous nucieatdpre trace clay and or nodules feldspar bituminous

85-2313B0.10-0.30 Ovoid pellets Compact 0.05-0.10 Quartzandcalcite Slightly - 20.3ArgillaceousCalcareous with 25 30% and very minorclay CXbonaCCOU lo quartzitic nucleated; 5.10% or phosphorite ao1ites;phosphate bituminous cement TABLE 15 CONTINUED

Sam ple Pellet Size NatureSize SamplePellet of PhosphateOrganicGanguePhosphate Gangue Size Iron Ca rbonateClassification Gr;!de N umber (mm) Phosphate DispersionPhosphate (mm) Number (mm) Content Content ContentReplacement (% hod

91 0.104.20 DispersedOvoidandoolitic 0.104.20 Mainly calcitewith Very minor CalcareousSlightlyPhosphorite 20 pellets with quartzandminor carbonate andcarbonaceious 50 60% nucleated clay lesser clay or some phosphatized bituminous biaclastic debris

90 1/4 0.20-0.30Ovoid pellets Compact 0.10-0.20 Mainlycalcite with Slightly CalcareousPhosphorjte 20.29 with 30 with 40% andlesser quartz carbonaceous nucleated or clay minor or encased;rare bituminous nodules;some phos phatized bio clastic debris

85 2313A 0.1On.30Ovoidpellets Dispersed 0.05; withcalciteMainly VeryCalcareousSlightlyArgillaceous minor 20.3 with 60% some 0.10 lesserquam and carbonate carbonaceous to quartzitic nucleated;few minor clay and or phosphorite oolites; rare feldspar bituminous compound pellets TABLE 16 TEXTURAL AND COMPOSITIONAL FEATURES OF THE ERNIE PHOSPHATE

SamplePellet Size Nature of GanguePhosphate Gangue Phosphate Organic Iron CarbonateCompositionGrade Number (mm)Number Phosphate Dispenion Size ReplacementContentContent (%P,Ol)

LIZ 0.2-0.3 Mainly ovoid Semicompact 0.2-0.3 Calcite with minor Very minor Slightly Calcareous: Phosphorite 24.71 pellets with50% to dispened quHz; very minor carbonate carbon- mostly nucleated; less albite and clay aceous or calcite than 5% oolitic bituminous pellets.

SBB86-3 0.1-0.3 Generally ovoid Compact to 0.05-0.1 Fine quartz with Minor Moderately Slightly Quartzitic 27.28 pellets with5% semi- lessercalcite, carbonate carbon- calcareous: to argil- nucleated dispened dolomite, feldspar, aceous or calcite with laCeO"S mica and clay bituminous minor phosphorite dolomite

SBB86-4 0.1-0.3 Ovoid pellets Compact to 0.05-0.1 Fine quartz with Minor Slightly calcareous: Quartzitic 22.33 with5-10% semicompact calcite and very serieite carhon- mainly phosphorite nucleated; rare minor feldspar and and clay aceous or calcite oolitic pellets clay bituminous

SBB86-6 0.3-0.5 Ovoid pellets Semi-compact 0. I Very fine-grained Minor Moderately caicareous: Quartzitic 13.41 with 25% to dispersed calciteand minor calcite with carbon- mostly phosphorite nucleated serieite and clay lesser acenus or calcite sericite and bituminous clay SBB86-I3 0.1-0.2 Ovoid peliets Semicompact 0.05-0.1 Mainly fine-grained Slightly Quartzitic 23.19 with less than to disoened auartz carbon- phosphorite 5% nucleated; aceous or rare oolitic bituminous pellet

SBB86-38 0.1-0.3; Ovoid pellets Semicompact 0.05-0.1 Fine-grained quam Weak Slightly Very weakly Phosphorite 25.27 Rare 0.5 with less than to dispersed and calcite; minor carbonate carbon- calca

SBB86-40 0.1-0.3 Ovoid pellets, Semi-campact 0.05 Slightly Slightly Phosphatic 7.29 intraclastsand to dispened carhan- ferrug- quartzose nodules; 5% aceous or inous siltstone nucleated bituminous

*, *, n.._.._:.:- 410 "3 SBB86-70 0.!-0.4 Owid ?!!et. Compzct tn 0.05 O.! Vev Oae-gnind Li!tk , ,O cl*.*lJ VY"Y,L& AO.7 with 5% nucleated semicomoact quartz with minor or carbon- to argil- feldspar and clay "One aceous or laceous bituminous phosphate TART-." " .E 17. . TEXTURAL AND COMPOSITIONAL FEATURES OF THE TOAD FORMATION PHOSPHATES

Sample Pellet Size Nature of PhosphateGangue Size Gangue OrganicPhosphate Iron ClassificationCarbonateGrade Number (mml Phosphate Dispersion (mm) ContentReplacementContent content

SB87-16(3) 0.10-0.30 Ovoid pellets Dispened to 0.05-0.10 Dolomite andquartz Slightly CalcareousPhosphorite33.34 with 50% semi-compact with lesserclay carbonaceous nucleated or bituminous

SB87-37(4) 0.05-0.10 Ovoidpellets Dispersed to 0.05-0.10 Calcite with lesser Highly 5.3 Calcareous I with 50% semi-compact quartz and minor carbonaceous nucleated dolomite; mce or feldspar and clay bituminous

SB87-40 0.05-0.15 Ovoid pellets Semicompact 0.05-0.10 Calcite andquartz Moderately CalcarCU 12.12 with 50.60% nucl- with minor dolomite carbonaceous eated orencased; and trace feldspar or bituminous rare nodule; phosphatized bioclastic debris

SB87-43 0.20-0.30Ovoid pellets Dispersed 0.10 Quartz with lesserSlightlyCalcareous toMinor 10.4 ~ with 50.60% calcite;minor moderate carbonaceous nucleated or dolomite carbonate Or encased bituminous floated effectively with fatty acid or anionic collectors. This tation of carbonate minerals, followed immediately by cat- is believed to be due tothe presence of montmorillonite in ionic flotation of silica. Results demonstrated the potential for the matrix. Recoveries from the Lizard deposits were seri- an increase of 12 to 15% in total phosphate recovery if the ously affected by its high carbonate content. A process of flotation process is incorporated into an existing witshing-siz- careful grinding, attrition-scrubbing and elutriation, gener- ing plant. Pilot plant tests achieved recoveries from flotation ally produced the best results at all three sites (J.M. Hamil- feed in the range of 73 to 96%. ton, personal communication, 1986; Christie and Kenny, in Studies on the beneficiation of Brazilian phosphate ores preparation); the best results were obtained for the Mount at The University of British Columiba (de Araujo el al., 1986) Lyne deposits. have indicated that desliming, using selective floccdation fol- Recent research has resulted in the replacement of tra- lowed by a conventional single-stage anionic flotation of ditional fatty acids by new collectors such as amphoteric phosphate, give the best results. alkyl aminopropionicacids.Thesedo notrequircphosphate depressants (Notholt and Highley,1986) and offer some en- Exploitation of phosphate deposits in British Columbia couragement for processing ores from areas where mont- will require beneficiation techniques that will prodm a con- morillonite is a problem. centrate grade of 30% P205 with acceptable recowries. All test work completed to datewas done on the Fernie phosphate In the mid-Sixties the United States Bureau of Mines more than IO years ago; new methods being developed may undertook a study of the Meade Peak member of the Phos- be more effective. Processes that have recently bem tried or phoria Formation (Town, 1967). This study is discussed here seriously considered include dense-medium oyclorte precon- in some detailas there are a number ofsimilarities between centration, high-intensity magnetic separation and selective pelletal phosphorites of the Phosphoria Formation and those leaching of dolomite from high-grade phosphorite:; (Hollick of the Fernie Formation, the Whistler member of the Sul- and Wright, 1986). This later process may be critical to the phur Mountain Formation and the Ishbel Group. beneficiation of the Whistler member phosphorite. Samples with initial phosphate grades ranging from 21.6 to 27.1% P205 were upgraded to over 31% P2os. A Recent work by Wilemon and Scheiner (1987: on phos- sample initially containing 15.3 % P205 and 17.4 % P205 phate ores in Florida suggest that the direct leachin;: of phos- after roasting was also upgraded to over 31 % P205 but re- phate rock using sulphuric acid and alcohol mixtun:s may be coveries were substantially lower. Samples in the 10 to 11% an alternative to beneficiation procedures previoudy tested. PzOs range were upgraded to 23% PzOs with recoveries of Phosphate recoveries as high as 90% were obtained in their only 71 % . studies. However, other investigations involving the same This study showed that the initial phosphate content is mixture had recoveries of only 60 to 65% (Wilson andRadan, the single most important factor affecting concentration. 1978). Themain problem with this process is obtainilg a prod- Calcite and dolomite started to decompose at approximately uct low enough in iron and alumina to meet feedstc~ckspeci- 700°C during roasting. A pH between 8.5 and 9.5 provided fications for fertilizermanufacture. the best conditions forflotation. Grinding finer than -65 or In the dry process, metallic phosphorus is produced by the -100-mesh had little effect; grinds finer than ..lSO-mesh thermal reduction of phosphate rock in an clectri: furnace caused lower recoveries because of slime losses while im- charged with calcined phosphate rock, silica and coke. The proving the concentrate gradeonly slightly. The amount of phosphorus is then oxidized to form P205 and rea:ted with emulsion required depended on the pellet size, percentage water toform a high-purity phosphoric acid. Much of the phos- of clay and sericite and the number of cleaning steps neces- phate rock produced from the Phosphoria Formation is proc- sary to obtain acid grade (31% PzOs). Flotation of silica essed this way. The major drawback is the high energy from phosphate resulted in higher phosphate losses and consumption in the initial reduction stage and therefme higher lower grade concentrates. cost. PhOSphdte rock used in this processgenerally has a grade Research on the beneficiation of phosphorite from the of 24 to 3% p205 (52 to 70% BPL) and an iron co.1tent less Phosphoria Formation is ongoing. Recent work by Judd ef than 1.5% Fe203. It should also have a water contenl less than al. (1986) has achieved 98% recovery of phosphate by 4%. In British Columbia, phosphate deposits occur close to leaching of unbeneficiated phosphate ores, but did not large deposits of coking coal and sources of hydr,,-electric evaluate the cost effectiveness of the procedure. Rule et al. power. Phosphate deposits in the Fernie Formation appear to (1982) also completed a study of flotation techniques on the meet the required criteria for the dry process and it can be Phosphoria phosphates. Their work involved depression of considered a possible alternative for processing British Co- the phosphate minerals with fluosilicic acid andanionic flo- lumbia phosphate ores.

Bulkfin 98 83 __- 84 Geological Survey Branch CHAPTER 8 RESOURCEPOTENTIAL OF' SEDIMENTARY PHOSPIHATE DEPOSITS IN BRITISH COL"I3IA

The economic viability of any mineral deposit is de- Phosphate resource potential has been (calculated for pendent upon many factors, including the size, grade and phosphate-bearing formations where practicable. 'The cal- geomeay of the deposit; mining and processing costs; the culations are based on broadly spaced sample sites and as- capital cost of development; and the cost of transportation sume continuity of grade and thickness along stlike and to market. Flat-lying phosphate deposits in Florida are down dip. As in MacDonalds's study, structural ccmplica- mined by low-cost open-pit methods and the ore is readily tionswerenotconsidered.Aspecificgravityof2.8v/asused concentrated, allowing Florida producerstoexploitdeposits for deposits with a grade greater than or equal to 12% PzOs with grades of less than 15% PzOs. The more geologically and 2.7 for lower grade deposits. These specific gravities complex deposits in Idaho and Montana require grades as are average values and may vary from the actual specific high as 30% Pzo5 to be economically viable as they are gravity at any given location. Summaries of the calculated mined both by open-pit and more expensive underground resource potentials are presented in Tables IS to 20. Phos- methods and beneficiation costs are also higher (see Chapter phate deposits are discussed in order from oldest to yonng- 7). est. Deposits with the best potential occur within the Substantial phosphate deposits are present in British Whistler member of the Sulphur Mountain Formation and Columbia butnone currently are economically viable. This at the base of the Fernie Formation. chapter will attempt to outline the phosphate resource potential throughout the province. A similar study of phos- CAMBRIAN OCCURRENCES phate deposits in Alberta has been completed by The only recorded Occurrences of phosphate in Cam- MacDonald (1987). MacDonald's parameters for estimat- brian rocks in British Columbia are at Mount Sheffield and ing resource potential are largely adopted here; estimates are in the Upper Cambrian Kechika Formation in the gicinity for in situ phosphate and economically recoverability is not of Grey Peak. The resourcepotential for Cambrian :strata is implied unless specifically stated. Detailed phosphate in- considered to be low. ventories have been calculated for some deposits, for the most part, these estimates remain confidential.

TABLE 18 RESOURCE POTENTIALFOR PERMIAN PHOSPHATES

Area FormationThicknessOutcropGrossArea Tonnes Grade (W Length (m) (x 106) (%PZOS)

I Johnston CanyonJohnston I 40 3 97.2 3-5 16.2 11 JohnstonCanyon 19 1 15.4 2.6 16.4 111Canyon Ranger 2s 1 20.3 3.4 8 IV Ranger CanyonRanger IV 38 1 30.8 5.1 4 V 120CondensedPermian 1 97.2 16.2 8.3 VI Mowitch 125 1 101.2 16.9 12.5 VI1 Mowitch 15 1 12.2 2 11.7

382 1.29* 373.3 62.4 8.4** TOTALS62.4 373.3 1.29* 382

Specific Gravity: 2.7 "Arithmetic Average **Weighted Average

Bulletin 98 85 TABLE 19 mented from the middle phosphate horizons and grades of RESOURCE POTENTIAL FOR TRIASSIC 15% or more across widths of IO centimetres or less are recorded from the uppermost phosphate horizon (MacC,on- PHOSPHATES ald, 1985). AreaFormation/ Outcrop Thickness Gross Tonnes Grade Exshaw exposures onMorrissey Ridge and in theFlat- member Length (m) (x 106) head River area ofBritish Columbia are restricted and were (%PZOS) (W 300111 50m .- not examined during this study. MacDonald (1985) recorded values of 0.28% P205 across a width of 1.5 metres I Whistler 140 1 113.4 19 15-20 and 0.16% PzO5 across 0.8 metre at Mount Broadwcsod. member West of the Elk Valley the Exshaw Formation is not exposed. MacDonald (1987) has calculated a resource polen- I1 FmToad 300 IO 4052430 5 tial of 10.4 million tonnes (down-dip 300 metres) or 1.7 I1 Subsurface: million tonnes (50 metres downdip)for the Exshaw Fonna- tion in Alberta. However, this phosphate occurs inarea: al- Area 200 x 50 = 100 OOO kmz ienated from explorationor development. Thickness: Averare- 20 m Sp. Gr. 2.7 PERMIAN DEPOSITS Resource Potcntial: 54 x lo9 tonnes of unknown grade JOHNSTON CANYON FORMATION Probably the best potential for Permian phosphate: in TABLE 20 southeastem British Columbia theis in JohnstonCan]ron RESOURCE POTENTIALFOR THE Formation. De Schmid (1917) suggests that a cantinu'ms BASAL FERNIE PHOSPHATE phosphate sheet may have been depositedat thebase of the Johnston Canyon Formation and although much of it has been removed by erosion, much has heen preserved. Both AreaOutcrop Thickness Gross TonnesGrade nodular and pelletal varieties are present. The resource Jo- Length (m) (x 106) (%05) tential of the Johnston Canyon Formation is estimatec: at (km) 300111 50m __ approximately 370 million tonnes grading somewhat less than 10% PzO5, to a depth of metres down-dip. Erti- 28 1.5 35.3I 1.5 28 5.9 19 300 mates are summarized in Table 18 and distribution of the I1 6.5 1.41.5 8.2 20 resource is shown in Figure 58. 111 12 17.5 1.5 2.5 15.1 IV 24 1 20.2 3.4 15 Along the MacDonald thrust fault in the Bighorn - V 12 9.5 20 57.1 3.4 Cabin Creek area at the southeastern limit of deposition of VI20 5.7 2734 1.5 the Johnston Canyon Formation, phosphate OCCUIS almost VI1 22 1 18.5 3.1 17.3 continuously. The thickness of phosphatic intervals vaies considerably, from less than 5 metres inthe southeast to 22 VI11 25.5 3.61 21.4 25 metres at Mount Broadwood. Northwesterly alongthe sa ne 10.7 1.5 13.5 2.3 17.5 Ix trend, in the vicinity of the Femie ski-hill, phosphatic inter- X 8 1.6 10.7 1.8 15.2 vals vary from 1 centimetre to 1 metre thick. Along this XI 20 1.5 25.2 4.2 15 trend, a basal conglomerate 25 to 30 centimetres thick con- XI1 56 1.511.8 70.6 17 tains chert and phosphate pebbles and hasa phosphate con- XI11 15 2.11 12.6 15 tent averaging 4.3% P205. At the Fernie ski-hill this Total 124.2 IS* 57.3342.4 1Gz conglomerate is only 1 to 2 centimetres thick. *Arithmetic average Pelletal phosphorite in the Johnson Canyon Formation **Weighted average **Weighted .- was recognized only in the Nordstrum - Brult5 - Weigzrt Creeks area. Work by the author and MacDonald (198:s) indicates the presence of at least one pelletal phosphorite EXSHAW FORMATION bed, ranging inthickness from 0.5 to 2 metres withthe phos- The Devono-Mississippian Exshaw Formation, al- phate content ranging from12.7 to 22.7% Pzo5. though phosphate bearing, does not represent a significant Nodular phosphorite occurs alonga strike length of 120 phosphate resourcein British Columbia but does have some kilometres on the eastern margin of Permian exposures. A potential in Alberta (MacDonald,1987). The best phosphate sample of nodules from an outcrop in the Crowsnest am exposures are restricted to the High Rock Range immedi- assayed 24.0% PzOs while a sample of sandstone from the ately north and south of CrowsnestPass. Many ofthe better same locality assayed 12.3%PzOs. This phosphate horizm, grade exposures are in Alberta. Grades of 1 to 9% Pz0s which is approximately 1 metre thick, can be traced as far across 10 to 30 centimetres have been reported from the south as Flathead Pass and as far north as Banff, where basal sandstone betweenPhillipps Pass and RacehorsePass. grades of 27.63% P205 have been reported (de Schm d, Grades of6 to 10% across widths of1 metre have been docu- 1917).

86 Geological Branch Survey Ministry of Employment und In vesfmenl

zons have yielded values up to 20%P205. Thicknesses over which these grades were obtained were only a fraction of a metre. There isalso littlecontinuity of these phosphate beds over significant distances. The potential for econc,mic deposits is considered to helow. RANGER CANYON FORMATION The RangerCanyon Formation is widely distributed. It is estimated to outcrop over an area of 150 000 sqlare kilometres in British Columbia and Alberta (F:apson- McGugan, 1970). In southeastern British Columbia phosphatic exposures are thickest along the wes:ern and southwestern margins of the Fernie basin where phosphate is present in a basal conglomerate and more comrlonly as nodules, although other forms are also present. F:esource potential for the Ranger Canyon Formation in British Co- lumbia is summarized in Table 18 and its distrihu':ion outlined in Figure 58. The best potential occurs in Alberta where MacDonald (1987) has estimated a potential for 230 million tonnes calculated downdip for 300 met~es,with grades in the range 6 to 18% PZo5. A phosphatic interval varying in thickness from 0.4 to 4metresoutcropsintheMutzCreek(12)-FairyC1eek(l3) (Figure 14) area north of Fernie. Phosphate content is low and is not considered economically significant. Thi!: horizon is believed to extend into the Hartley Creek(15) (Fi,gure'14) area. Norris (1965) also reports the presence of phosphate nodules in the uppermost Ishbel Group from a locality 5 kilometres east of Mount Proctor. Because of sparse data, no resource potential was calculated for this area. To the west, near the Fernie ski-hill, a phosphate bed assays 13.3% P205 across 0.5 metre and is the best occurrence in this area. A well-defined phosphatic bed is present in the upper part of the Ranger Canyon Formation in the Connor Lakes area. A sandstone bed, 1 metre thick and containing phos- N phate nodules averaging 6 centimetres in diameter, occurs I on the limbs of a series of anticlinal and syncha1 folds. Although this bed has an extensive strike length and the phosphate nodules contain in excess of 25% P205, the bed as a whole (including the nodules) average:; less than 5% p205. Figure 58. Resource potential for Permian phosphates, The phosphate resource potential of the Ranger Canyon southeastern BritishColumbia. Formation in southeastern British Columbia appears to he limited, approximately 20 million tonnes with a gr;.de of 8% The best potential in the Johnston Canyon Formation Pzo5 orless. Most of the areas examined contain cxtensive appears tobe in the Nordstrum - Weigert Creek area (Area occurrences of low-grade phosphate (less than 2% P205 11) and along the MacDonald thrust (Area I), hut estimating across thicknesses of 1 to IO metres). tonnage and grade is difficult. While grades in excess of In northeastern British Columbia phosphilte is re- 12% Pz05 are present, continuity along strike isalmost im- stricted to a bed 1 metre thick at the top of the Mowitch possible to ascertain as the structure in this area is relatively Formation or stratigraphically equivalent Fantasque Forma- complex. tion, extending from Meosin Mountain tosouth of Lemoray (Areas VI and VII, Figure 59). Phosphate is nodular and ROSS CREEK FORMATION grades are in the order of 12% PzO5. The Ross Creek Formation is restricted in its distrihu- Phosphate is present in the subsurface in the BclloyFor- tion and phosphate is known at only a few localities. Phos- mation of the Peace River district (roughly equivalent to the phatic intervals tend to be low grade (lessthan 5% Pzo5) and Ishhel Group of southeastern British Columbia) hut at are generally less than 1 metre thick. MacRae and McGugan depths that preclude its inclusion in estimates of resource (1977) report that samples collected from phosphate hori- potential. This horizon extends eastward into Albxta.

__" Bulletin 98 87 ~ ~~ ~ ~ ~.~~ ~~~~~~~~~~ ~~ 16) represents a potential source of sedimentary phospbate Sampled locality ...... 0 second only to the Femie Formation in the East Koote!lav Permian stmta (may include district. At Meosin Mountainthis bed is 1.3 metres thick;mb Pennsylvanian and consists of both pelletal and nodular phosphate. Sou& of Mississippian ...... ;:.,:8~s,... - Meosin Mountainthis bed passesinto phosphatic, bioclastic 80 and silty limestone and phosphatic calcareous siltstone. A Kilometres phosphorite bed 1 to 2 centimetres is present at I&mo~.ay, north of Watson Peak. However,its exact stratigraphic position is uncertain. The resource potential for the Whistler member phosphorite is estimated to be 113 million tonnes containing 15 to 20% PzOs. Within this belt the best potential is southeast of Wapiti N Lake where the hoststratigraphy has been foldedinto series I of plunging synclines and anticlines (Heffernan, 1980; Legun and Elkins, 1986). Here the phosphorite range; in r

12C 122 J .~

Figure 59. Resource potential for Permian phosphates, northeastem British Columbia.

TRIASSIC DEPOSITS Phosphate Dccurrences in Triassic strata extend from the Alberta - British Columbia boundary near Kakwa Lake to north of the Alaska Highway westof Fort Nelson. Areas of resource potential are shown in Figure 60 and resource estimates summarized in Table 12219. 12c A phosphorite bed,occurring at or near the base of the Whistler member of the Sulphur Mountain Formation and Figure 60.Resource potential for Triassic phosphates, extending from Meosin Mountain to Watson Peak (Figure northeastern British Columbia.

88 Geological Survey Brmch Ministry of Employmen1 and Irvestment

thickness from 0.8 to 3.2 metres with assays varying 11.9 to Although these deep depositsrepresent a significantre- 23.7 P205 (Heffernan, 1980; A. Legun, personal communi- source, the possibility of exploiting them in theforeseeable cation, 1987). Phosphorite is exposed on a dip slope on the future is extremely remote. eastern limbof the Wapiti syncline, placing large tonnages potentially within reach of surface mining. The base of the phosphorite bed is marked by a thin phosphatic conglomer- FERNIE FORMATION ate that vanesin thickness from 5 to 20 centimstres. Phosphate occurring at the base of the Fernie Formation represents the best potential for developing an economic de- SUBSURFACE TRIASSIC DEPOSITS posit in the foreseeable future. It can be traced along strike for approximately kilometres in Southeastern British Subsurface phosphate of Triassic age can be traced as 300 far north asFort Nelson. Near Fort Nelson the Triassic thins Columbia. and the phosphatic sequence pinches out. Depths to the top Phosphate is present as a single bed, or as two beds of the phosphatic unit vary from 547 to 2015 metres with separated by phosphatic shale, throughout thc Fernie basin the greater depthsgenerally occurring in the most easterly and is consistently at least 1 to 2 metres thick (Figure 61), of the holes examined. The phosphate interval varies from locally attaining thicknesses of 2 to 3 metres. As lnuch as a few metres to in excess of 300 metres thick. Correlation 8.4 billion tonnes of phosphate rock may have beet1 depos- with surface phosphate occurrences shows a general thick- ited, but less than 5% of this can be considered a potential ening in the vicinity of Richards Creek and extending south- resource. The gross resource potential is estimated to be342 easterly in the subsurface. This thickened interval covers million tonnes with a grade between 11 and 29% €205 and only a small area as it quickly thins in every direction, most averaging 17% PzOs. A down-dip extension of 300 metres noticeably easterly where the Triassic section as a whole has been used in thiscalculation. Resource potential for spe- decreases in thickness. cific areas outlined in Figure 62 is summarized in Table 20.

Phosphote (numbers congtomerote refer to 5: P*O,) 0Sandatone timertone %ole Siltrlone

silly dolomite Calcareaur shale Limertone, conglamerote a interbedded rhole tlnd riltrtone Phosphatic...... P __ Figure 61. Stratigraphic correlationof the basal Fernie phosphate in Southeastern BritishColumbia.

Bulletin 98 89 Thrust faulting has thickened the phosphate bed at some localities and atothers, the phosphate has been renlohili ~ed into the noses of folds (Hartley, 1982). Phosphate conterd is in the range of 13 to 20% P205; less silty varieties conlain more than 20% Pz05 (Hartley, 1982). The Cabin Creek area is estimated to have a resocrce potential of 34 million tonnes, calculated to a depth of :300 metres, with an average grade of approximately 2Q%P!O5. There is some untested potential immediately west of the Flathead River in the vicinity of Cabin Creek. North of Crowsnest Pass, the Crow deposit has been the subject of extensive underground work and metallurgical testing by Cominco Ltd. It has an estimated resource po:en- tial in excess of 2 million tonnes with an average grads: of approximately 25% P205. This same phosphate bed is interpreted to extend to the headwaters of Alexander Cteek where grades averaging 28.4% P205 across widths of 0.3 metre or less have been sampled. In the westLine Creek area the basal phosphate can be traced for a strikelength of 15 kilometres, in strata that dip 40 to 75 degrees easterly. It varies in thickness from less than 1 metre south of Line Creek, to more than 3 metres at Mount Lyne. Phosphate content ranges from a low of 3.7% P205 in a diamond-drill hole, to ahigh of23.7%PzO5 across 1.6 metres in a backhoe trench (Hannah, 1980). At M~~unt Lyne the phosphorite averages 22.9% p205 across 2 mc:tres or 19.8% P205 across 3 metres. Crows Nest Resources Ltd. calculated a reserve of 972 800 tonnes to a depth of 30 metres in the ,west Line Creek area, based on a strikelength of 5850 metres ani an average thickness of 2 metres (Hannah, 1980). The resource potential of the Line Creek area is estimated to be in excess of 25 million tonnes with a grade of approximately :LO% PzOs, assuming a strikelength of 15 kilometres, an average thickness of 2 metres and a depth of 300 metres. The estimated grade is based on surface samples and therefore cmld be lower, depending on how much weathering of the phosphate has taken place. In the Barnes Lake area phosphorite is exposed along the limbs of a sequence of folds. The phosphate resource potential for the Fernie Formation in this area is estixated to be 7million tonnes to a depth of 100 metres, based on a 25.5-kilometre strike length and an average thickness of 1 metre. An additional 4.2 million tonnes may be availat leto the east of the Corhin logging road. Figure 62. Resource potential for the Ferniephosphate, Christie (1981; in preparation) has suggested that “nor- southeastern British Columbia. mative apatite” or “hone phosphate of lime” could be cilled “total formational apatite” (TFA) andexpressed in centimetres by the formula: The southeastern and eastern exposures of the basal TFA = thickness (metres) x assay (% PzOs) x 2.18. phosphate appear to offer the best economic potential. The Under ideal conditions, “total formational apatite” can southeasternmost exposures ofthe basal phosphate occur in be usedto indicate where apatite formed, that is, which parts the Cabin Creek area. Exploration by First Nuclear Corpo- of the basin are most phosphogenic. This procedurc, al- ration Ltd. (Hartley, 1982), Imperial Oil Ltd. (Van Fraassen, though it will not show where the phosphate is economic, 1978) and the author has demonstrated continuity of a phos- can he useful in locating target areas within a phospho1:enic phate bed averaging 1.5 metres in thickness along a strike region that may contain economic phosphate. length of 27 kilometres. Phosphate is present in a broad syn- Total formational apatite (TFA) has been ca1culatc.d for clinal structure modified by thrust faults and minor folds. several localities in the Fernie basin: the results are shown

90 Geologicul Survey Brunch Ministry of Employment and In mtmmf

in Figure 63. Their distribution confirms that the eastern 1 margin of the basinis the most phosphogenic, and thatthere are two centres of more intense phosphogenesis, the Cabin Creek and Crowsnest Pass areas. A single value ai: Mount Lyne southeastofElkfordsuggeststhatphosphogen4:sis was also active in this area. It should be noted that for those localities where the section is incomplete, the calculated value is a minimum. These results tend to confirm the hy- pothesis that the eastern margin of the Fernie basin offers the best potential for economic phosphate deposits Carbonatite deposits also represent a significar t source of phosphate in the province, with the Aley deposit account- ing for virtually all of the resource potential. Its vesource potential is estimated in excess of 30 billion tonnes. Phos- phate could conceivably be produced as a byproduc t should this property be brought into production for niobium.

J Figure 63. Total formational apatite, basal phosphate horizon, Fernie Formation.

Bulletin 98 91 .- ___ 92 Geological Survey Branzh CHAPTER 9 SUMMARY ANI) CONCLUSIONS

British Columbia is well endowed with phosphate de- The phosphate potentia1 of Permian strata is dif ticult to posits, both sedimentary and igneous. Sedimentary phos- assess because of the predominantly nodular natur,: of the phate deposits have been identified in 14 stratigrpahic units phosphate. While the nodules may contain in excess of 25% ranging in age from Upper Cambrian to Lower Jurassic. PzOs and canoccur over stratigraphic thicknesses of several These deposits areall located in the Rocky Mountains east metres, the host beds have phosphate values pmerzlly less of the Rocky Mountain Trench. Some isolated occurrences than 2 to 4% PzOs. occur west of the trench but none are of economic signifi- Two areas of pelletal phosphorite, Weigert an(l Nord- cance. Sedimentary phosphate occurs in a variety of forms strum Creek appear to have limited areal extent a.though but only pelletal varieties offer potential for futuredevelop- phosphate grades are in excess of 12 and 24% respectively. ment. Grades greater than 15% PzOs, the threshold of eco- These deposits cannot be considered as having a hrge re- nomic interest, occur only in the Whistler member of the source potential. The Ranger Canyon Formation in British Sulphur Mountain Formation, in the Femie Formation and Columbia is estimated to have a resource potential of 51 locally in Permian strata. At present these phosphate depos- million tonnes with grades between 4 and 8% PzOs. its cannot competewith production from the westem United In northeastern British Columbia the bestpotential for States where beds grading 30% PzOs are selectively mined. Permian phosphateis in theMowitchFormation where there In the future, as production in Florida decreases and mining is an estimated potential for 113 million tonnes with a phos- of lower grade phosphate from the Phosphoria Formation phate grade averaging approximately 12% Pz05. becomes necessary, phosphate deposits in British Columbia may become economically viable. Presently known deposits in British Columbia present Triassic: practical difficulties with respect to their mining and bene- Phosphate deposits of Triassic age include predomi- ficiation. Phosphate beds are narrow and their structural at- nantly nodular varieties in the Toad Formation and xlletal titude precludes open-pit mining in mostlocations. The low phosphorite in the Whistler member of the Sulphur Moun- grade of these depositsrequires that they be beneficiated to tain Formation. The Toad Formation may have a rf:source meet fertilizer industry standards. While past research on potential in excess of 2 billion tonnes with grades of :1 to 5% beneficiation of these deposits has not been particularly re- PzOs. The Whistler member is estimated to have a resource warding, more recent work offers some encouragement. potential of 113 million tonnes with grades of 15 I:O 20% PzOs, assuming the best possible parameters. Inchlded in this resource is the potential for approximately 11 010 ton- Cambrian: nes of lanthanum and 4500 tonnes of cerium. These depos- Phosphate deposits of Cambrian age occur primarily in its, because of their high carbonate content, &'resent the Kechika Formation as thin beds of limited areal extent. beneficiation problems in addition to difficult minirbg con- They do not represent a significant resource potential. Pres- ditions. Although most of these deposits would have to be ently known phosphate occurrences are located in mined underground there appears to be some open-pit po- Kwadacha Provincial Park and are precluded from explora- tential in the Wapiti Lake area. tion. A large phosphate resource of undetermined grzde and dubious exploitability is present in Triassic strata in tksub- Mississippian: surface. Phosphate deposits of Mississippian age are present in Jurassic: the Exshaw Formation. The best resource potential for these deposits is in Alberta immediately adjacent to British Co- The best potential for an economic sedimentary phos- lumbia, north ofCrowsnest Pass. These deposits too are pre- phate deposit occurs at the base of the Jurassic Femie For- cluded from development as they occur in an Alberta mation. This phosphorite bed is estimated to have a Protection Area. maximum resource potential of 340 million tomes grading 15 to 20% Pzo5. It is also estimated to contain approximately 66 000 tonnes of lanthanum, 44 000 tonnes of ce- Permian: rium, 163 000 tonnes of yttrium and ll 000 tonnes of Phosphate deposits are present in several stratigraphic uranium and represents a significant source of these ~netals. units of Permian age. These depositsare best developed in Beneficiation of the Fernie phosphate will require southeastern British Columbia, in strata the Johnston Can- grinding to either 65- or 100-mesh depending on grain size, yon and Ranger Canyon formations. desliming to remove the clay fraction and flotation. Calcin-

Bulletin 98 93 ing will he required in areas where the carbonate or organic Carbonatitesalso represent a significant source of content is high. Exploration Of these deposits should-con- phosphate intheprovince. Atpresenton&theAley centrate on the eastern and southeastern margin the Femie of tite has significant phosphate potential. Other phosphate- Basin. Phosphate grades and, to some extent,trace element cOntenaare generally higher in these while tt,e car. hearing carbonatites do occur and the potential for locating honate content tendsbe to muchlower. more of these depositsexcellent. is

94 Geological Suwey Branch Aaquist. B. (1981): Blue River Carhonatites, British Columbia, Northeastern British Columbia, Geological Survey ofcan- Final Report 1981,B.C. Ministry of Energy, Mines andPe- ada, Paper 79-1A, pages 219-226. troleum Resources, Assessment Report 10274,30 pages. Cheney, T.M. (1957): Phosphate in Utah and on Analysis of the Altschuler, Z.S., Clarke, R.S. and Young, E.J. (1958): Geochem- Stratigraphy of the Park City and Phosphoria Fomations, istry of Uranium in Phosphorite, United States Geological Utah, Utah Geological and Mineralogical Suwey,E:ulIetin Survey, Professional Paper 314D, pagcs 45-90. 59,54 pages. Altschuler, Z.S. (1980): The Geochemistry of Trace Elements in Christie, R.L. (1978): Sedimentary Phosphate Deposits - An In- MariuePhosphorites. Part1. Characteristic Ahundancesand terimReview, GeologicalSurveyofCanada,Paper7&20,9 Enrichment, The Society of Economic Paleontologists and pages. Mineralogists, Special Publication No. 29, pages 19-30. Christie, R.L. (1980): Paleolatitudes audPotentia1for Phosphorite Armstrong, J.E. (1949): Fort St. James Map-area, Cassiar and Deposition in Canada, Geological Survey of Canada, Paper Coast Districts, British Columbia, Geological Survey of 80-IB, pages 241-248. Canada, Memoir 252,210 pages. Christie, R.L. (1981): Phosphoritein Westem Canada, Carodiarr Bamkr, E.W., Taylor, G.C. and Proctor, R.M. (1968): Carhonif- InsrituteofMiningandMetallurgy,ReprintNumber55,83r~l erous and Permian Stratigraphy of Northeastern British Co- Annual Gcneral Meeting, Calgary, May 4-7, 1981. lumbia, Geological Survey of Canada, Paper 68-15, 25 Christie, R.L. (in preparation): Phosphogenic Basins and Phos- pages. phate Economicsin the Cordilleran Region of Western Can.. Barry, G.S. (1986): Phosphate, Canadian Minerals Yearbook, ada, Geological Survey of Canada. 1987, pages 46.1-46.8; Energy, Mines and Resources Can- Christie, R.L. and Kenny, R.L.(in preparation): Phosphate Explo. ada. ration in theSouthem CanadianRockies,Canadian6istitute Mining and Metallurgy. Barry, G.S. (1987): Phosphate,Canadian Mining Jounzal, Fehm- of ary 1987, pages 65-66. Cook, P.J. (1976): Sedimentary Phosphate Deposits,in Hardhook of Stratahound and Stratiform Ore Deposits, Volume”, K.H. Benvenuto, GL. and Price, R.A. (1979): Structural Evolution of Wolf, Editor, Elsevier, pages 505-535. the Hosmer Thrust Sheet, Southeastern British Columbia, Canadian Petroleum Geologists, Bulletin, Volume 27, Cook, P.J. and McElhinney, M.W. (1979): A Reevaluation of the Number 3, pages 360-394. Spatial and Temporal Distribution of Sedimentary Phos- phate Deposits in the Light of Plate Tectonics, Economic Burnett, W.C., Beers, M.J. and Rock,K. (1982): Growth Ratesof Geology, Volume 74, pages 315-330. Phosphate Nodules from the Continental Margin off Pem, Science, Volume 215, Number 26, pages 1616-1617. Dales, G.D. (1978): Report on Diamond Core Drilling - FH and WW Group Claims,B. C. Ministry of Energy, Mines andPe- Butrenchuk, S.B.(1987a): Phosphate Inventory (82G andI), B.C. troleum Resources,Assessment Report 6859. Ministry of Energy, Mines and Petroleum Resources, Geo- logical Fieldwork, 1986, Paper 1987-1, pages 289-302. de Araujo, A.C., Poling, G.W. and Cwlho, E.M. (1986): Selective Dcsliming of Sedimcntary PhosphateOres, Canadian Insti- Butrenchuk, S.B. (1987h): Phosphate Deposits of Southeastern tuteofMiningandMetallurgy,Bulletin,Volumc79,Number British Columbia. B.C. Ministry ofEnerg3 Mines and Pe- 895, pages 52-59. tmleum Resources, Open File 1987-16, 103 pages. de Schmid, H.S. (1917): A Rcconnaissance for Phosphatein the Butreuchuk, S.B. (1988): Phosphate Inventory: Northeastern Brit- Rocky Mountains: and for Graphite near Cranhrook, 13ritish ishColumhia,B.C.MinistryofEnergy,MinesandPetroleum Columbia, Deportment of Mines, Mines Branch, Ottawa, Resources, Geological Ficldwork, 1987, Paper 1988-1, Summary Report, 1916, pages 22-35. pages 396410. Dorian, N. (1975): Refraction Seismic Survcy on the Flahead Campbell, R.B., Mountjoy, E.W. and Young,F.G. (1973): Geology Phosphate Claims,B.C. Ministry of Energ3 Mines and Pe- of McBride Map-area, British Columbia,GeologicalSurvey troleum Resources, Asscssment Report 5556. of Canada, Paper 72-35, 104 pages. Douglas, R.J.W., Gabrielse, H., Wheeler,1.0.. Stott, D.F. and Be- Cann, R.M. and Godwin, C.I. (1983): Genesis of Magmatic Mag- lyea, H.R. (1970): Gedogyof WesternCanada, in Gdogy netite-apatiteLodes,lronMaskBatholith,SouthcentralBrit- and Economic Minerals of Canada, Chapter VIII,Grologi- ish Columbia (921). B.C. Minisrrv of Enerav. Mines and calSurveyofCanado,EconomicGeologyReport1,5thEdi- Petroleum Res&ces, Geologica

Bulletin 98 95 hills, Geological Associationof Canada, Proceedings,Vol- Henderson, G.G.L. and Dahlstrom, C.D.A. (1959):First-order ume 20, pages 76-87. Nappe in Canadian Rockies, Bulletin of American Associa- Gabrielse, H., Dodds, C.J., Mansy, J.L. and Eisbacher, G.H. tion of Petroleum Geologists, Volume 43, Numhcr 3, pages (1977): Geological Mapof Ware West Halfand ToodopAone 641-653. River Map-areas,Geological Survey of Canada, Open File Hollick, C.T. and Wright, R. (1986): Recent Trendsin Phosphite Report 483. Mineral Beneficiation,The Institutionof Mining undMetd- Gibson, D.W. (1969): Triassic Stratigraphy of the Bow River - lurgy,Transactions, Section A, Mining Industry,Volume 55, Crowsnest Pass Region, Rocky Mountains of Alberta and July 1986, pages A150-Al54. British Columbia, Geological Survey of Canada, Paper 68- Hoy, T. (1987): Geology of the Cottenbelt Lead-zinc-magnette 29,49 pages. Layer, Carbonatites and Alkalic Rocksin the Mount Gm:e Gibson, D.W. (1971): Triassic Stratigraphy of the Sikanni Chief Area, Frenchman Cap Dome, SoutheasternBritish Colum- River - Pine Pass Region, Rocky Mountain Foothills, North- bia, B.C. Ministry of Energy, Mines and Petroleum Re- eastern British Columbia,Geological Survey of Canada, Pa- sources, Bulletin 80,99 pages. per70-31,105pages. Irish, E.J.W. (1970): Halfway River Map-area,British Columb.a, Gibson, D.W. (1972): Triassic Stratigraphy of the Pine Pass - Geological Survey of Canada, Paper 69-1 1,154pages. Smoky River Area, Rocky Mountain Foothillls and Front Irving, E. (1979): Paleopoles and Paleolatitudesof North America Ranges of British Columbia and Alberta,Geological Survey and Speculations ahout Displaced Terrains,Canadian J0L.r- of Camda, Paper 71-30,108pages. nul of Earth Sciences, Volume 16, pages 669-694. Gibson, D.W. (1974): Triassic Rocks of the Southem Canadian Judd, J.C., Sandberg, R.G. and Huiatt, J.L. (1986): Recovery of Rocky Mountains, Geological Survey of Canada, Bulletin Vanadium, Uranium and Phosphate from Idaho Phosphor:te 230,65 pages. Ores, United States Bureau of Mines, Report of Investiga- Gibson, D.W. (1 975): Triassic Rocks of the Rocky MountainFoot- tions 9025, 15 pages. hillsandFrontRangesofNonheasternBritishColumbiaand Kazakov, A.V. (1937):The Phosphorite Facies andthe Gcnesis of West-central Alberta, Geological Survey of Canada, Bullc- Phosphorites, in Geological Investigations of Agricultulal tin 247.42 pages. Ores of the U.S.S.R., Science Institute, Fertilizers and ln- Gwdfellow, W.D. and Jonasson, I.R.(1983): Environment of For- secto-Fungicides,Transactions, Volume 142, page!$95-113 mation of the Howards Pass (XU)Zn-Pb Deposit, Sclwyn (published for thc 17th International Geological Congrelzs, Basin, Yukon, in Mineral Deposits of Northem Cordillera, Leningrad). J.A. Morin, Editor;Canadian Institute of Mining and Met- Kenny,R.L.(1977):PhosphateExplorationinSoutheasternBritiih allurgy, Special Volume 37, pages 19-50. Columbia, ComincoLtd., talk presented at Meeting, Cana- Grove, E.W. (1986): Geology and Mineral Depositsof the Unuk dian Instituteof Mining and Metallurgy,Ottawa, Ontario. River-SalmonRiver-AnyoxArea,B.C.MinistryofEnergy, King, D.E.C. (1986): Rare Earths, Canudian Minerals Yearbo,?k Mines ond Petroleum Resources, Bulletin pages. 63, 152 1986, Review and Outlook, Mineral Report35, pages 50.1- Gulbrandsen,R.A. (1966): ChemicalCompositionofPhosphorites 50.10. of the Phosphoria Formation, Geockimica and Cosmo- Kouloheris, A.P. (1977): Solving Problems in Chemical Procers- chimica Acta, Volume 30, pages 769-778. ing of Low Quality PhosphateRock Engineering nnd Min- Halbertsma, H.L. (1959): Nomenclaturc of Upper Carboniferous ing Journal. pages 104-108. and Permian Strata in the Subsurface of the Peace River Krauskopf, K.B. (1955): Sedimentary Deposits of Rare Metals, Area, Journal Alberta Society Petroleum Geologists, of of Economic Geology, 50th Anniversary Volume, pages 411- Volume Number 5, pages 7, 109-118. 463. Hannah, T.W. Phospahtic Bedsin the Formation of (1980): Fernie P.H. Vanadium Mineral CommodityProfile, Unit'zd West Linc Creek, Southeast British Columbia, Crows Nest Kuck, (1983): States Bureau Mines, pages. Resources Ltd.,Unpublished Company Report. of 18 Lavers, W. Phosphate Rock Regional Supplyancl Chang- Hartley, G.S. Physical Work and Investigation of Miner- (1986): (1981): ing Pattern of World Trade, The Institution Mining and alization on the Zip1 Claim, B.C. Ministry Energy, Mines of of Metallurgy, Transactions, Section A, Mining Industry, VW and Petroleum Resources, Assessment Report9142. ume 95, July 1986, pages AI 19-Al25. Hartley,G.S. (1982): Investigation of PhosphateMineralizationon the Cabin Creek Claims 1-45 and on the Zip 1 Claim, B.C. Leech,G.B.(1960):Fernie(West-hal~,GeologicalSurveyofCan- ado, Map MinistryofEnergy,MinesandPelmleumResources,Assess- 11-1960 (1:126720). men1 Report 10135. Leech, G.B. (1979): Kananaskis Lakes,West Half, British Colurn- bia and Alberta 1?2), GeologicalSurveyof~ana~a, Hartman, F.H. and Wyman, R.A. (1974): Beneficiation of Phos- (82J/W phate Rock from Fernie, British Columbia,Energy, Mines Open File Map 634 (]:I25OOO). and Resources Canada, Investigation Report IR74-37, 22 Legun, A. aand Elkins, P. (1986): Wapiti Syncline PhosphatePo- pages. tential, B.C. Ministry of Energy, Mines und Petroleum Re- sources, Geological Fieldwork, Paper pag:s Heffernan, K.J. (1978): 1977Drilling Report for Lodge 1 Claim 1985, 1986-1, 151-153. in the Fort Steele Mining Division,B.C. Ministry of Energy, Mines andPetroleum Resources, Assessment Report'7616. Mabie, C.P. and Hess,H.C. (1964): Petrographic Study and Clas- sification of Western Phosphate Ores,United States Deparr- Heffernan, K.J. (1980): Report on Geological Mapping, Sampling and Drilling, Wapiti 1-25 Claims, B.C. Ministry ofEnergy, mentoftkeInterior,ReportofInvestigations6468,95pagr:s. Mines and Petroleum Resources, Assessment Report 8407, Mxder, U.K.(1987): The Aley Carbonatite Complex, Northem 17 pages. Rocky Mountains,British Columbia (94B/5),B.C. Ministry

96 Geological Survey Bran:h of Energy, Mines and Petroleum Resources, Geological Pell, I. (1985): Carbonatites and Related Rocksin British Colum- Fieldwork, 1986, Paper 1987-1, pages283-288. bia; in Geological Fieldwork 1984,B.C. Ministry of hergy, McCrossan, R.G. and Glaister,R.P. (1964): Geological History of MinesandPetmleumResources,Paper1985-1,pager 84-94.. Western Canada, Alberta Society of Petmleum Geologists, Pell, 1. (1987): Alkaline Ultrabasic Rocks in British Columbia: 232 pages. Carbonatites, Nepheline Syenites, Kimberlites, Ulb.amafic MacDonald, D.E. (1985): Geology and Resource Potential of Lamprophyres and Related Rocks;B.C. Minisfry of ,?nergy, Phosphates in Alberta and Portionsof Southeastern British Mines and Petmleum Resources, Open File 1987.: 7, 109 Columbia, UnpuhlishedM.Sc.Thesis,UniversityofAIberta, pages. 238 pages. Pelletier, B.R. (1961): Triassic Stratigraphyof the Rocky Moun- MacDonald, D.E. (1987): Geology and Resource Potential of tains and Foothills, Northeastern British Columbia [91K and Phosphates inAlbena,Alberta Research Council,Earth Sci- N (partsof)]; Geological Surveyof Canada, Paper 61-8,3% ences Report87465 pages. pages. McGugan, A. (1967): Permian Stratigraphy, Peace River Area, Pelletier, B.R. (1963): Triassic Stratigraphyof the Rocky Moun- Northeast British Columbia,Canadian Petroleum Geology, tains and Foothills, Peace River District,British Columbia, Bulletin Volume 15, Number 1, pages 82-90. Geological Survey of Canada, Paper 62-26.43 pages. McGugan, A. andRapson, J.E. (1962): Permo-Carbonikrous Stra- Pelletier, B.R. (1964): Triassic Stratigraphyof the Rocky Moun- tigraphy,CrowsnestArea,AlbertaandBritishColumbia,Al- lain Foothills Between Peace and Muskwa Riven, North- berta Societyof Petroleum Geologists, Journal, Volume IO, eastern British Columbia, Geological Survey of Canada, pages 352-368. Paper 63-33,89 pages. McGugan, A. and Rapson,J.E. (1964a): Permian and Carbonifer- Pelzer, M.A. (1977): Geological and Drilling Report, 1977Field ous Stratigraphy, Crowsnest Area, Alberta andBritish Co- Work, Phosphate Properties, Flathead Area,British Colum- lumbia, Canadian Petroleum Geologists, Bulletin, Volume bia, B.C. Ministry of Energy, Mines and Petrolerrm Re- 12, Field Conference Guidebook, pages 494-499. sources, Assessment Report 6365. McGugan, A. and Rapson, 1.E. (1964h): Pemo-Carboniferous Pettijohn, F.J. (1957): Sedimentary Rocks, Second Edition: New Stratigraphy,Wapiti Lakearea, Northeast BritishColumbia, York: Harper and Row, 718 pages. B.C. Ministry of Energy, Mines and Petroleum Resources, Pilcher, S.H. (1983): Report onthe Geology and Geochemi( al Sur- Assessment Report 1155 (Petroleum ResourcesDivision). veys and PhysicalWork Conducted onthe Ren I, 11, I11 and MacIntyre, D.G. (1980): Geological Compilation andMineral Oc- IV Claims, KamloopsMiningDivision: B.C. Ministq,ofEn- currence Map, Driftpile Creek- Aikie River, B.C. Ministry ergy, Mines and Petroleum Resources, Asscs:imcnt Report of Energy, Mines and Petroleum Resources, Preliminary 11639, 17 pages. Map 38. Price, R.A. (1961): Fernie (East-half),GeologicalSurvey~~Can- MacIntyre, D.G. (1981): Akie River Project (94F),B.C. Ministry ado,Map35-1961 (1:126720). of Energy, Mines and Petroleum Resources, Geological Price, R.A. (1964): Flathead (Upper Flathead, East Half),British Fictdwork, 1980, Paper 1981-1, pages 33-47. Columbia - Alberta, Geological Survey of Canadfc, Map MacIntyre, D.G. (1982): Akie River Project (94F),B.C. Minisfry 1154A, (150 000). of Energy, Mines and Petroleum Resources, Geological Price, R.A. and Grieve, D. (in preparation): Tornado Mountain, Fieldwork, 1982-1, pages 142-148. British Columbia and Alberta,(150 OOO), Geologicd Sur.. McMechan, M.E. (1987): Stratigraphy and Structureof the Mount vey of Canada. Selwyn Area, Rocky Mountains, Northeastern British Co- Price, R.A. and Grieve,D. (in preparation): FordingRiver, British lumbia, Geological Survey of Canada, Paper 85-28, 34 Columbia and Alberta (150 040). Geological Suivey of pages. Canada. MacRae, J. and McGugan, A. (1977): Permian Stratigraphy and Pmd’hommc, M. and Francis,D. (1987): The FertilizerIndustry, Sedimentology - Southwestern Alberta and Southeastern Eneqy, Mines and Resources Canada, Mineral Polky Sec- British Columbia, Canadian Petroleum Geologists, Bulle- tor, Intcrnal ReportMRI 8713, 15 pages. tin, Volume 25, Number 4, pages 752-766. Rapson-McGugan, J.E.(1970): The Diagenesis and Dcpor,itional Newmarch, C.B. (1953): Geology of the Crowsnest Coal Basin Environment of the Permian Ranger Canyonand MJwitcb with Special Referenceto the Fernie Area,B.C. Ministry of Formations, Ishbel Group, from the Southern Canadian Energy, Mines and Petroleum Resources, Bulletin 33, 107 Rocky Mountains, Sedimentology, Volume 15, pagf s 363.. pages. 417. Noms, D.K. (1965): Stratigraphy of the Rocky Mountain Group Rule,A.R.,Larson,D.E.andDallenbach,C.B.(1982):Application in the Southeastern Cordilleraof Canada, Geological Survey of Carbonate-silica Flotation Techniques toWestern Phos-. of Canada, Bulletin 125, 82 pages. phate Material, United Stores Bureau of Mines, Report of Notholt, A.J.G. and Highley, D.E. (1986): World Phosphate Re- Investigations 8782, 13 pages. sources, with particular reference to Potential Law-grade Russell, A. (1987): PhosphateRock TrendsinProcessing andPro- Ores: The Institution of Mining and Metallurgy, Transac- duction, Industrial Minerals,Number 240,Septembr 1987, tions, Section A, Mining Industry, Volume 95, July 1986, pages 25-52. pages 125-132. Savanick, G.A. (1983):New Developmentsin HydraulicBc,rehole Patton, W.W. and Matzko, J.1. (1959): Phosphate Deposits in Mining of Phosphate, in Phosphates: What I’rospe:ts for Northern Alaska,United States Department of the Interior, Growth?, P.W. Harben, Editor, Metal Bulletin Inc., New Geological Survey Professional Paper 302-A,16 pages. York.

Bulletin 98 97 Sheldon, R.P. (1981): Ancient Marine Phosphorites, Annual Re- Thompson, R.I. (1986g): Mount Robb,GeologicalSurveyof Cm- view of Earth Planetary Science,Volume 9, pages251-284. ado, Map 7-1986. Sheldon,R.P.(1987):AssociationofPhosphaticandSiliceousMa- Thompson, R.I. (3986h): Mount Laurier, Geological Survey of rine Sedimentary Deposits, in Siliceous Sedimentary Rock- Canada, Map 8-1986. hosted Ores and Petroleum, J.R. Hein, Editor, pages58-80. Town, J.W. (1967): Petrographic and Flotation Studies on the Slansky, M. (1980): Meade Peak, Idaho, Phosphate Samples,United Sfares L'e- partment of the Interior, Bureau of Mines, Reportof Invcs- Slansky,M.(1986):GeologyofSedimentaryPhosphates,EIsevier, tigations 6751, 15 pagcs. 210 pages. Van Fraassen, M.A. (1978): 1978 Drilling and Geology Repcrt, Smik, L.C. (1988): Smctural Geology of the Cariboo Gold Min- Cabin 1, 2, 3, and Ram 1 and 2 Claims, B.C. Ministry of ing District, East-central British Columbia,Geological Sur- Energy, Mines and Petroleum Resources, Assessrncnt Re- veyof Canada, Memoir421.100 pages. port7617. Taplin, A.C. (1967): Internal Company Report,Cominco Lrd. Wehhcr, G.L. (1975): Geological Report on Grave Lake Groups Taylor,G.C.andStott,D.F.(1973):TuchodiLakesMap-area,Geo- No. 1 and No. 2, B.C. Minisrry of Energy, Mines and Petro- logical Survey of Canada, Memoir 373,37 pages. leum Resources, Assessment Report 5545. Telfer, L. (1933): Phosphate in the Canadian Rockies,Canadian Wehhcr, G.L. (1976): Diamond Drilling Report on Grave Lake Inslitufe of Mining and Mefallurgy, Transactions, Volume Group No. 1, B.C. Ministry of Energy, Mines and Petrole~!m 36, pages 566-605. Resources, Assessment Report 5545. Thompson, R.I. (1986a): Mount Brewster and Jones Peak, Geo- Werner, A.B.T. (1982): Phosphate Rock an Imported Minel.al 1agicalSurvey of Canada, Map 1-1986. Commodity, Energy, MinesandResourcesCanada, Mimal Bulletin, MR193,61pages. Thompson,R.I.(1986h): WickedRiver,GeologicaISurveyofCan- a&, Map 21986. Wilemon,G.M. and Scheiner,B.J. (1987): Leachingof Phosph<.te Values from two Central FloridaOres using H*SOd-mefi,a- Thompson, R.I. (1986~):Gauvreau Creek, Geological Survey of nal Mixtures,Unired Srares Deparrmenr of theInterior, Re- Canada, Map 3-1986. port of Investigations9094,9 pages. Thompson, R.I. (1986d): Emerslund Lakes and Hackney Hills, Wilson, R.A. and Radan,D.J. (1978): Phosphoric Acid Manufsc- Geological Survey Canada, Map 4-1986. of lure from Phosphate Matrix,Unites States Patent 4,105,74 9, Thompson, R.I. (1986e): Christina Falls, Geological Survey of August 8,1978. Can&, Map 5-1986. Young, G.A. and Uglow, W.L. (1926): TheIron Ores of Canaca; Thompson, R.I. (19860: Mount Lady Laurier, Geological Survey Geological Survey of Canada, Economic Geology Series, of Canada, Map 6-1986. Number 3, pages 109-128.

98 Geological Survey Branch GLOSSARY OF TERMINOLOGY

USED IN THIS REP0:RT”-

Pellet: Phosphategrain no greater than 4.0 millimetresin Phosphate Term applied to phosphate-bearingrock It at is longest dimension. Rock minedand used as a rawmaterial inthe manufacture of phosphate fertilizers. Nodule: Phosphategrain4.0millimetres or morein longest dimension. Phosphorite: Adepositofphosphaterockofsedinientaryorigin, which is of economic interest. It is generally Ovoid Pellet: Pellet with no discernible internal structure assumed that the rock containsa minimumof 18% P205 or 50% apatite hy volume. Forpuqoses of Oolite: Pelletwith concentric internal strnctures. this report the term phosphorite is applied:.o those rocks having a pelletal texture and containing NucleatedPellet hat has a centre of non-phosphalic material greater than 7%P20.5. Pellet: with adiameter of less thanone-half the minimum diameter of the pellet. Bone PhosphateExpression of thecalcium phosphate Phosphate content of phosphate rock (equivalent to 2.1852 x Polynucleated Pellets containing twoor more detrital grains or of Lime (BPL): % P205). Pellet: fossil fragments. Phosphatic Rock with arenite grain size that contains I to 5% Encased Pellet with core-diameterequal to orgreater than Pellet: halfof theminimum diameter ofthe pellet. Sandstone: P20.5.

Intraclasts:Reworked fragment of a contemporarysediment Phosphatic Rock with rudite grain size that conrains 1 to 5% from the same depositional basin. Shale: P20.5.

CompactedTexture in whichmore than one-half ofthe fluor-Phosphatic Rock with silt grain sizethat contains 1 to 5% Texture:apatite occurs as pellets that are mostly adjoining.Siltstone: P205.

SemidispersedTexture in whichone-half of thefluorapatite Desliming: The process of removingclay material fiom the Texture: occurspelletsas thatonly are partially adjoining. rock.

DispersedTexture in whichgangue is dominantor where Flotation: Proccss used to produce a product ranging ;iom 70 Texture: greaterthan one-half of thefluorapatite occurs to 72% BPL. interstitially as pellets.

Bulletin 98 99 British Columbia " Ministry of Employment and Innl'estment

APPENDICES "-

Bulletin 98 101 British Columbia __

.- __ 102 Geological Survey Branch Minisfry of Employmenr and Inv?sfmenr

APPENDIX 1 CALCULATIONS USED TO DETERMINE MINERALOGICAL COMPOSITION USED IN TIHE CLASSIFICATION OF PHOSPHATE ROCKS

In Mahieand Hess’s (1964) classification the following In our classification we make the same basic assumptions assumptions were made: exceptthatweassumethatthefluorapatitecont;lins40percent PzOs by weight. In addition we adda carbonate anda I organic (I) All the PzOs was assumed to be in the form of collo component. Calculations are based on the following formula: phane obtaining 38 per cent PzOs by weight. (2) Alumina was assumed to be in the form of muscovite- (1) Quartz and muscovite-sericite-clay were calculated in a sencite-clay containing 38.5 per cent A1203 by weight. similar manner to that of Mahie and Hess. (3) All Si02 not inmuscovite-sericite-clay was assumedto (2) Fluorapatite = 2.5 x wt. % P205. be in quartz. (3) Organic matter = 1.2 x wt. % Corg (from Gibson, 197.5). (4) Carhonate=1.78x[wt.%CaO~ota~-(1.32r.wt.SbPzOs)]. Mineralogical components werecalculated as follows: As with Mahie and Hess our classification does not ac- (1) Fluorapatite (collophane) = 2.63 x wt. % PzOs. count for minor amounts offeldspar or dolomite that may be (2) Muscovite-sencite-clay = 2.60 x wt. % A1203. present. Many of the phosphorites thein western UnitedStates (3) Quartz = wt. % Si02 - (1.17 x wt. % Alz03). contained fluorapatite with 39 to 40 per cent P20s by weight. For fluorapatite the ratio of 1.32/1 for CaOPzOswas used in calculating the amount of CaO required for fluorapatite.

Bullerin 98 10.7 APPENDIX 2 MAJOR OXIDES - KECHIKA AND ROAD RIVER FORMATIONS

(l)S66738(1) 34265 MwntSheffidd11.24 0.31 68.6 0.08 3.94 1.55 1.6 1.070.99 10.78 0.160.29 0.25 0.970.01 1.02 11.15 - - (l)SE87 39 34266 Grey Peak1.74 2.49 42.17 16.91 18.61 0.07 2.161.26 0.1715 0.080.06 0.27 1.50. I 1.62 14 2.26 0.34 (Z)SE67 39(1) 34267(Z)SE6739(1) aey Peek 5.1366.27 0.29 0.24 2.74 3.978.04 0.2 4.62 0.06 6.39 0.53 7.760.06 0.16 0.27 2.66 - (l)SE673W2) 34268 GreyPeak.18 EO77 10.45 14.6 1.16 3.5 2.63 11.652.19 0.08 0.35 0.3 0.22 0.06 0.04 2.7113.86 0.28 62.17 5.51 8.71 5.02 0.19 5.2 3.07 5.2 0.19 5.02 8.71 (2)56875.51 39(4)34269 62.17Grey Peek 0.28 0.34 0.080.04 0.28 7.21 3.140.34 8.97 0.57 - - (2)SE87 3q5) 24270Grey Peak 1.14 4.240.85 8.08 66.07

(1) KechikaFmaticn (2) Road RNw F~matiim 'R&=Fe&h+N&,+h!gO

APPENDIX 3 MAJOR OXIDES - PERMIAN PHOSPHATES

Sample Lab LoCasaO P*Or So, QO MA Fe2& Me0 MgO 60 Ti02 MnO Co? COR1 F Hz0 S LM FeO MO Ith' Number Numbw - (1)SE- 32980 Femie Ski Hill 14.630.130.57 0.27 59.590.15 0.31 1.62 20.47 0.2911.69 0.20.01 0.25 0.63 0.68 2.11 Od 0.15 (1)SEEffi 17 32982ML Eroadwmd 1.65 79.14 5.57 1.990.7 2.63 0.17 0.55 0.180.74 7.98 0.02 0.16 0.238.7 0.16 0.293 0.38 3.13 ~l)SEE6641 32984 Cabin Creek 2.7 66.16 6.95 364 0.72 0.06 1.474.44 0.31 0.04 10.19 0.560.050.19 0.26 10.38 0.43 0.31 3.26 (1)SEEffi57 32985 WeilerfCreek 14.71 16.66 43.65 0.251.57 0.31 0.660.06 0.15 0.04 27.35 1.2 1.11 0.240.292 21.26 0.28 0.96 0.17 (1)SEB%62 32985 FwsVmCreek 3.21 61.92 1.4612.85 0.690.47 5.83 0.05 0.11 14.050.13 1.18 0.29 0.32 13.070.16 0.251 0 2.49 (1)SEE6571 32986 Cromnesl Pass 14.41 M.18 20.490.06 0.17 1.06 0.660.89 1.79 0.02 0.07 0.33 0.19 0.23 0.14 1.440.08 0.42 0.211 (l)SEE6679(1) 32989 NMdSPDmCteek 24.59 37.41 33.90.35 0.76 1.5 0.24 0.48 0.11 0.010.501 1.77 0.352.42 0.21 1.43 1.26 0.38 0.11 (1)SEBffiW 32990 MacDcnald Fault 0.44 50.83 4.826.48 1.160.45 1.41 0.M 0.030.18 39.M 0.1 5.15 0.3926.13 1.41 0.5 " (2)S887 GW 33510 Montana 0.5244.9 9.05 34.3 0.06 0.05 0.28 0.1 0.020.02 1.44 0.39 r2.00 0.3512.02 0.12 0.06 1.31 0.02 (2)5867 G(2) 33511 Mcntana 2.0347.41 8.74 33.7 1.1 0.1 0.020.35 0.07 0.39 2.2 0.6 >2.W4.510.74 0.73 0.18 0.1 1.41 (3)SSs7 37 34261(3)SSs7 37 Richaids Creek 0.07GO.10 0.5 0.04 1.46 0.1295.62 0.a 0.06 0 0.261.35 0.04 0.32 0.090.4 1.38 " (4)SE6745 34355 Alaska Hlghway2.060.27 1.17 4.94 26.71 29.88 4.5 1.3 0.21 32.850.03 4.M 0.37 0.77 26.500.22 0.38 6.38 1.61

(1) 1ShtMGrap APPENDIX 4 MAJOR OXIDES - TRIASSIC PHOSPHATES (values in per cent)

Sample Lab Locatim P20, Si& CaO Al& Fez% Na20 MgO bo Ti& MnO c& Cog F H,O S LOI FeO CaO R$Ii

SB87 6 33503 M-5" Mwntii 23.54 2.49 48.94 0.37 0.12 0.27 0.54 0.13 0.02 0.03 32.7 5.05 72 0.41 0.54 2001 0.3 1.71 0.03 SB87 714) 33504 Me~sinMounhin 5.01 18.74 42.68 0.46 0.17 0.06 0.61 0.19 0.02 0.02 34.5 3.41 0.34 0.22 0.36 0.2631.M 8.52 0.29 33505 Wapiti Lake 26.39 15.98 44.54 1.15 0.33 0.34 0.65 0.35 0.07 0.03 11.1 2.22 72 0.530.26 9.81 0.33 1.69 0.08 33506 Wapir Lake 26.3 11.63 47.13 0.68 0.16 0.19 0.88 0.18 0.W 0.03 12.2 2.74 72 0.46 0.35 0.229.83 1.66 0.05 33507 Mwnl Palsm 28.02 10.74 44.87 1.74 0.54 0.15 0.98 0.7 0.08 0.02 13.5 1.91 72 0.65 0.079.98 0.25 1.6 0.12 SB87 16(3) 33508 LWnaaY 33.34 4.91 47.73 1.96 1.W 0.59 0.69 0.45 0.16 0.01 5.57 1.17 72 0.U 0.8 0.235.21 1.43 0.11

SB87 19 35502 Lemotay 0.38 05.96 4.07 1.49 0.48 0.02 0.5 0.3 007 0 7~05~~ ~ 1.23 0.06 0.320.24 5.87 0.28 - - SB87 1911) 33509 LemWaY 1.11 66.91 11.- 2.55 0.72 0.32 0.39 0.46 0.11 0.01 15.1 2.03 0.18 0.45 0.2412.090.39 3.3 10.49 SB67 32~ 34252 west Bvml titer 0.51 25.15 30.79 3.69 0.94 0.45 2.94 1.23 0.18 0.03 45.7 7.01 0.07 0.22 33.40.91 0.M SB8732(1) 34253 West Bum1 tiier 1.14 77.15 6.82 1.63 1.15 0.01 2.71 0.51 0.1 0.01 7.1 , 0.68 0.19 0.35 0.w 8.36 0.35 5.98 4.82 SB87~. 34 34255 Mwnlludi~lm 0.31 50.39 16.47 8.99 1.75 1.11 2.82 1.84 0.42 0.03 20.06 2.01 0.06 0.20 17.670.27 0.86 - -

SB87 34(2) 34256 MwnILudingtOO 8.37 29.32 30.1 4.16 0.61 049~~ ~ 2.M 1.03 0.2 0.03 27 6.16 0.49 0.3 0.13. ~..233 0.67. 3.6 0.84 SB67 35 34257 Mwnlludinglm 14.4 11.58 46.6 1.25 0.62 0.41 0.81 0.21 0.05 0.W 23.74 2.94 1.35 0.35 0.1 0.2922.36 3.24 0.19 588736" 34258 Lavder Pasri Nm 0.08 59.49 l0.M 9.35 1.84 1.03 1.34 2.44 16.160.03 0.53 2.9 0.07 0.6 13.210.11 0.96 - - SB87 36(1) 34259 Lautier Pass N& 7.26 29.25 30.75 4.88 0.77 0.49 1.47 1.29 0.23 0.02 31.3 4.46 0.62 0.8 0.05 23.95 0.430.43 4.23 34260 Lautier Pes Nm 29.52 9.17 47.36 0.82 0.24 0.21 0.55 0.12 0.03 0.03 0.14 4.69 72 0.05 0.3 11.39 0.29 1.6 0.05

34262 RlchadsCreek 0.87 47.35 12.75 6.09 6.14 0.84 3.94 1.96 049 0.09 m9~.~" 1.29 0.11 0.32 1.17 1635.." 2.92~ - - 34263 tiiad%Creek 4.62 46.53 19.55 605 1.31 0.62 2.24 1.52 0.34 0.02 20.87 3.55 0.41 0.5 0.46 16.6 0.57 4.23 2.07 SB8737(4) 1.1534264 0.06 RichadsCreek0.37 2.06 38.53 19.2 5.31 0.54 0.080.05 0.020.49 36.32 7.M 0.2132.810.55 7.26 0.67 SB8740 34271 Alaska Hlghway0.26 0.91 39.46 26.63 12.12 0.050.05 0.4 0.96 1.020.02 2.1 22.15 0.4 20.14 0.24 0.21 - - SB8743 34272 Alaska Hlghway0.09 0.53 0.75 45.07 15.77 10.4 0.88 0.030.23 0.1626.19 0.32 0.25 0.020.96 2.35 23.26 4.33 0.2 SB8743(1)34273 0.45 1.43iUaska 0.12 Hghway 0.41 1.77 31.16 39.85 9.98 0.0817.39 0.01 0.6 0.63 0.18 0.36 16.3 0.24 - -

' R& = Ala% + Fer% = NO IfPhosphatenodules APPENDIX 5 MAJOR OXIDES - FERNIE PHOSPHATE (JURASSIC)

Sample Lab Locatim p.01 Si& CaO AlA FeO, NaiO MgO iG0 X% MnO C& Gq F Hi0 S LM FeO CaO Ita, Nvmbet Number Pa03 P>%

LP. 32976 LkWc 47.7810.16 24.71 1.04 0.62 0.25 0.65 0.050.29 1.44 0.M1.05 21.22 0.02 0.541.93 0.43 14.09 0.08 SBB88 3 32977 Hlghhway 3 27.26 1.38 0.431649 0.29 1.9143.13 0.292.09 2.22 0.3415.81 0.02 0.09 0.36 6.68 0.S 1.58 0.13 SB8884 32978 crow 22331.83 0.2941.0711.97 19.64 0.16 0.44 1.23 1.6316.45 1.90.03 0.090.34 0.33 1.47 0.4 0.17 SBB86 6 32979 Fading tiww 13.41 16,s 1.9939.29 0440.2 0.94 0.44 0.082.91 30.27 0.03 0.85 0.3 21.150.57 0.36 0.252.92 SBB66 11 33276 island Lake 12.16 23.71 36.01 1.11 0.43 0.26 0.67 0.12 0.07 0.07 24.29 1.62 1.1 0.21 0.49 20.87 0.24 3.12 0.18 SBW 130 32981 Abby 23.19 35.08 34.11 1.69 0.42 0.39 0.43 0.38 0.07 0.02 7.M 1.53 1.38 0.42 0.31 4.71 0.33 1.47 0.11

15 33277SBB88~~~~~ 15 ZID 31.08 14.03 40.94 3.12 0.83 0.17 0.58 1.31 0.17 0.04 5.06 1.M 2 0.83 0.16 3.93 0.22 1.32 0.15 SSB8633282 22 0.58LakeHamel 2.4 2.29 8.62 5.6970.23 3.89 0.360.54 2.380.03 0.56 3.390.36 0.24 0.5 0.8 1.46 2.95 58856 37 33278Creek Cabin 41.3812.26 32.01 1.9 1.03 0.W0.12 0.79 0.431.29 0.5 5.52 0.59 0.45 0.052 2.67 10.76 0.1 SB886 35 Cabin33279 Creek 20.1625.27 2.5913.45 0.04 0.16 0.95 3675 0.78 0.12 1.01 2.62 1.957.57 0.59 0.4 0.28 0.171.45 5888640 32983 Cabin Creek 74.65 7.29 10.22 2.49 0.5 1.18 2.36 0.030.22 0.41 0.87 0.32 0.6 0.2 0.19 0.552.W 1.4 0.29

SB88642~~~~~ ~ 33280 Bahan 18.79 4541.21 2.82 26.44 0.09 1.190.35 0.410.27 1.75 0.350.68 3.67 0.03 2.65 0.35 0.231.41 SBW33283 52 Sixm Creek 2.9640.29 14.34 26.96 1.01 0.06 0.66 2.1313.650.9 0.05 0.12 0.25 2 0.86 8.190.17 1.49 0.26 5888654 33284 Cabin Creek 3.49 81.9 5.13 3.48 1.27 0.28 0.49 1.16 0.41 0.04 2.17 0.52 0.43 0.23 0.28 2.26 0.19 1.47 1.5 SB88670 32987 Llne Creek 28.43 20.51 38.33 3.59 0.88 0.31 0.66 1.3 0.19 0.02 8.03 2.4 1.69 0.6 0.32 5.37 0.36 1.35 0.18 SBW86 33281 Lodoe 27.34 21.55 36.89 4.13 1.19 0.1 0.65 1.38 0.2 0.34 6.11 1.17 2 0.62 0.16 4.59 0.28 1.35 0.22

Average 2.83 32.67 31.08 20.48 0.88 0.4 0.650.16 0.74 1.43 0.W1.63 11.46 1.67 0.35 0.397.95 0.39 044

'RA = Ale% + Fez% + NO APPENDIX 6 TRACE ELEMENTS - KECHIKA AND ROAD RIVER FORMATIONS

Sample C1 Ni Cr Y Rb Y AS Ba Au Pg Zn CU PbMO C4 u m seh ce vsc NmbR %( ppm ) W) ( ppm 1

(1~873241)221 35 12

(1)Avwage 21 3539 578 39 9.5 7w a0 ~0.5 102 zz io 20 ci 42 26 1 150 M 56 20.9 12)nuerage cO.01 24 12)nueragecO.01 38 144 19 19721 8.2 40 c0.5 55 24 9 4

(I)Kedika Fm. (2) Roal Rner Fm. NIA- NM anatyzed

APPENDIX 7 TRACE ELEMENTS - PERMIAN PHOSPHATES

cu pb MOC~Um se ta ce v ppm

13 8 7 Cl 23 Cg 3.1 113 €0 93 946 18.3 I 11 5 c5 3 4 4 3.7 28 27 20 1238 3.2 ~ 10 7 c5 1 4 7 <1.0 81 65 84 2197 7.2

28 12 c5 1 39 4 235 2.1 (€a 38 551 39 ~ 12 4 C5 1 23 8 3.1 38 23 87 74110.5 1 13 10 13 c5 4 88 8 1.5 M 90 80 14478 ,

20 14 <5 cl 103 9 4.7 133 90 210 860~ 25~5 ~ 13 46 1 8 11 6.1 33 27 77; 68 151028.2 22 9 7 371.5 6.5 3.1 91 €6 98 1E5 18 '1 i 11 153 c5 1 24 78 1 131 43 181 18743.6 j 21 28 23 2 155 14 23 476 78 279 €03 46.6 S887 37 14 37 S887 50 40 3 2375 42 QO35 <0.5 10 7 <8 NA 27 25 9 1817 23 NA 0.4 I SB8745 N4 NA 1343 NA 2745 20 NA 33 2718 13 10 40 15 391 2.7 C10 40 MO NA NA i

'Samplefmn he mospmia Formation at warn Spmgs. Mmtsna I ?R. No'nz?;:ed APPENDIX 8 TRACE ELEMENTS -TRIASSICPHOSPHATES

(1)SB676 *.01 42 ND 655 138 40 310 QO 0.6 13w 13 11 cg 42 116 12 6 13 43 469 - 24 42.7 (1)6887-7(4) 0.M 10 ND 351 11 40 644 QO 0.1 758 25 15 c5 16 55 9 13 5 43 532 212 40 37.2 (l)S887 11(2) -0.01 25 ND 435 329 C40 94 QO C0.5 280 14 14 <5 17 145 2 7 01 47 317 597 40 37.5 (l)SB67 12 -0.01 15 ND 516 452 40 52 QO <0.5 552 15 14 s5 26 193 26 5 167 69 287 333 40 40.6 (1)se8715 co.01 38 ND 636 246 40 141 <20 0.7 29w 46 14 10 91 96 9 16 82 44 445 693 38.9 14 (3lSE87 1631 c0.01 61 ND ZsO1 498 <40 339 *20 1.2 333 27 17 10 7 139 26 9 e4 17 114 1535 40 42.4 (2)SB67 19 a01 30 74 166 2 24 6 328 QO <0.5 83 20 11 <5 3 22 7 16 33 23 80 NA NA 3.2 (2)6B67 19(1) -0.01 40 e4 385 8 5 40 576 -3.0 0.5 191 M) 10 7 2 NID NID 20 0 12 198 765 40 12.3 (2)SB67-32 co.01 130 167 382 41 41 20 152 QO <0.5 15w 56 12 7 26 51 3922 22 31 1620 NA NA 26.9 (2)SB87 32(1) co.01 22 126 106 6 49 4.5 176 c20 C0.5 98 9 7 4 2 29 c5 10 59 44 41 NA NA5 (2)SB87 34 -0.01 45 115 220 46 18 17.6 -2 QO ~0.5 48 32 15 9 1 29 20 55 31 37 438 NA NA 16.9 (2)sewx:2) co.01 76 220 €63 41 42 6.1 2929 QO 3-z 49 12 7 1 M 38 32 33 26 474 NA NA 27.2 (z)se87 s co.01 17 59 676 19 17 5 61 -20 <0.5 21 10 5 3 Fl 42 42 5 3 NID 52 NA liA 38.f (2)SB8735 co.01 46 126 399 79 16 284 1393 QO 2 47w 62 13 34 67 30 34 24 38 218 2448 NA NA 39.2 (2)SB87 3w1) co.01 72 225 776 41 42 7.1 1460 <20 230 45 12 30 3 35 14 30 25 129 1026 NA NA 12 (2)SB67 3w2) 0.02 Jo 47 1709 27 104 4 746 QO a.5 627 26 3 8 10 26 Nm 11 31 52 215 NA NA 43.3 (2)SB8737(1) co.01 29 e4 165 49 31 20 416 QO 2 29 35 13 <8 Cl 23 cg 21 40 61 199 NA NA 15 (2)SB87 37(2) co.01 52 61 427 43 €4 9 670 QO 1 253 39 12 4 -1 32 12 6 61 e4 107 NA NA 19 (2)SB67 37(4) co.01 54 176 12M 43 90 10.2 800 QO 1 277 24 107 6 19 1257 57 255 16 1819 NA NA 33.6 (2)586740

Average 736

(1)~inUerMmber%lphurMarntain Fwmatim (2)Torxl Fmatim (3)Tilassic-Fmatim Uncertain NA - Not Analyzed NID - Not Detected APPENDIX 9 TRACE ELEMENTS - FERNIE PHOSPHATE (JURASSIC)

22 e43 i/ 516 1.3 119 40 COS 31 75 4 7 1 42 15 2.3 216 122 33 461 46 31 15?4 c7 351 1 676 QO <0.5 58 43 6 7 1 33 c6 1.3 108 91 45 912 47 40 1270 <7 326 3.9 747 QO

Average 42 - 765 460 <30 497 QO a5 8613 37 <5 0.9 33 6 3.2 195 130 63 lJBl - NIA - NotAnaiv2ed APPENDIX 10 SAMPLE LOCATIONS AND RESULTS FROM SOUTHEASTERN BRITISH COLUMBIA

S am ple Lab Latitude Longitude Age Longitude Latitude Lab Sample Formation Wdth p205 cu Pb Zn Number Number (N) (W (metres) ('4 @pm) (ppm)

SBB86 1A 31768 49"30'40" 115-05'30 Jurassic Fernie 0.7 0.59 12 6 48 SBB86 18 31769 49'3040" 115"05'30" Jurassic Fernie 1.o 0.75 io 5 51 I;

SBB86 IC 31770 49"30'40" 115'05'30" Jurassic Fernie 0.7 0.7 9 8 39 ~

SBB86 1D 31771 49'3040" 115"05'30 Jurassic Fernie 0.7 0.66 8 9 135 ~ SBB86 2A 31772 49"31'02' 115'06'00" Permian Ranger Canyon0.53 0.4 6 4 69 , SBB86 3A 31773Triassic 114"44'10 49'3915 Sulphur Mountain 0.7 0.33 14 18 150 SBB86 38 31774 49-39'15'' 114"44'10 Jurassic Fernie 0.5 21.322 38 639

SBB86 3C 31775 49'3915 114"44'10' Jurassic Fernie9.05 0.7 118 19 41 ~ SBB86 3D 31776 49"39'15 114"44'10" Jurassic Fernie 2.07 0.7 12 12 24 ??'$'44':0" SBB86 3E 31777 43"39'15" Fernie Jurassic 1.2 4.13 59 22 252 i~ SBB86 4A 31778 49"3945 114"42'30" Jurassic Fernie 1 26.6 44 20 126 SBB86 48 3 1779 49-39'45 114"42'30" Jurassic Fernie 1 2226.6 41 SBB86 4C 31780 49'3945 114'42'30' Jurassic Fernie 1 25.727 40 241IB0 I SBB86 4D 31781 49"3945 114"42'30 Jurassic Fernie 1 25.1 40 25 175

SBB86 4E 31782 49"39'45" 114"42'30" Jurassic Fernie 0.7 27 40 22 108 ~ SBB86 6A 31783 114"5055"49"54'20 Fernie Jurassic 22.7 0.4 41 17 58886 6B 31784114"50'55" 49"54'20" Fernie Jurassic 15.5 0.4 37 26 10575 ,1 SBB86 6C 31785 114'50'55"49"54'20" Jurassic Fernie 0.5 6.05 44 14 91

SBB86 6D 31786 4934'20 114'50'55 Jurassic Fernie 0.24 127.88 38 156 ~ SBB86 6E 31787 4954'20 114"5055 Jurassic Fernie 0.6 4.1812 36 141 , SBB86 6F 31788 49'54'20' 114'5055" Jurassic Fernie 0.4 1.92 24 8 57 SBB86 6G 31789 49Y4'20" 114"5055 Jurassic Fernie 0.6 1.3 16 9 84 58886 6H 31790 49'54'20' 114"50'55" Jurassic Fernie 1 0.61 67 22 208 SBB86 78 31921 49-53'20" 114"57'00" Permian Ranger Canyon grab 0.69 8 8 18

*PzOsAnalyses done by XRF Error f 1% Absolute for values Remaining P205samples analyzed by volumetric method S686 8A 31922 49-27'40 115"08'30" Permian Johnston Canyon 0.9 1.53 6 12 159 SB86 88 31923 49'27'40" 115'06'30" Permian Johnston Canyon 0.5 1.65 13 25 300 S686 8C 31924 49"27'40" 115"06'3O Permian Johnston Canyon 0.6 1.04 11 64 330 S686 8E 31925 49"27'40" 115"08'30" Permian Ranger Canyon 0.5 0.64 43 14 366 S686 8F 31926 49027'40 115"06'30" Permian Ranger Canyon 0.5 0.19 17 14 186 SB86 6H 31927 49"27'40* 115"08'30" Permian Ranger Canyon 0.3 0.08 6 12 133 SB86 6K 31928 49"27'40" 11 5'06'30" Permian Ranger Canyon 0.5 13.3 12 11 24 5886 8L 31929 49927'40- 115-08'30" Permian Ranger Canyon 0.7 2.38 5 8 24 S686 9A 31930 49"32'02 115'04'55'' Permian Ranger Canyon 1 1.77 9 24 59 SB86 9B 31931 49'32'02" 115"04'55' Permian Ranger Canyon 1 0.92 6 11 54 S686 9C 31932 49"32'02 115"04'55 Permian Rangercanyon 1 0.29 11 13 108 S686 9D 31933 49"32'02 115"04'55" Permian Ranger Canyon 1 0.35 10 9 120 '$903" n.3 'e--<."40" S686 IOA 3 1634 I 4"' ,,a I" I".!"rassic %Tie gras 13.2 28 I? !I7 SB86 11A 31935 49"31'50" 115'10'45" Jurassic Fernie grab 15.4 25 20 69 SB86 12 31936 49'58'50" 114"48'40" Jurassic Fernie grab 0.1 36 20 24 S686 13A 31937 50"18'25 114"56'05 Jurassic Fernie 0.35 7.43 26 14 39 SI386 136 31938 50"18'25 114'56'05 Jurassic Fernie 1.5 21.7 46 19 60 SB86 13C 31939 50'18'25" 114"56'05 Jurassic Femie 1 29.4 35 20 72 S686 14A 31940 50"12'00" 115"OO'OO Jurassic Fernie 1.04 1411.8 31 77 S686 146 3194j 50"12'00" 115°00'O0 Jurassic Fernie 0.65 1.48 28 15 66 S686 14C 31942 50'12'00" 115"OO'fW Jurassic Fernie 0.85 1.79 28 10 60 SB86 14D 31943 50"12'00" 115"00'00" Jurassic Fernie 1 0.16 54 17 78 S886 15A 31944 49"16'05 114'36'00" Jurassic Fernie 0.7 23.9 43 23 108 5686 156 31945 49"16'05" 114"36'00" Jurassic Fernie 0.7 27.1 40 27 121

5886 15C 31946 49"16'05~~ 114"36'00"~~ Jurassic~ ~.~ Fernie 13 8.46 31 13 103 S686 15D 31947 49"16'05" 114"36'0O Jurassic Fernie 27.1 121 0.7 27 40

*P205Analyses done byXRF Error f 1% Absolute for values Remaining P205samplesanalyzed by volumetric method Sa m ple Lab Latiude Lab Sample Age Longitude Pb Formation Width p205 cu Zn Number No. (N) (W (metres) (%)(ppm) (ppm) (ppm)

SBB86 17A 31948 49"18'00" 114Y6'55' Permian Johnson0.52 Canyon 0.3 13 10 15 SBB86 178 31949 49"18'00" 114"56'55" Permian Johnson Canyon 1 0.2. 11 16 60 SBB86 17C 31950 49"18'00" 114"56'55" Permian Johnson Canyon 1 0.66 13 11 105 SBB86 17D 31951 49'18'00" 114"56'55" Permian Johnson Canyon 1 0.35 23 14 216 SEE86 17E 31952 49"18'00" 114"56'55" Permian Johnson Canyon 1 1.72 15 12 360 SBB86 17F 31953 49"18'00" 11456'55" Permian Johnson Canyon 1 1.49 18 17 204 SBB86 17G 31954 49"18'00" 114'56'55" Permian Johnson Canyon 1 0.67 19 17 264 SBB86 17H 31955 49'18'00" 114-56'55 Permian Johnson Canyon 1.4 1.11 16 10 132 SEE86 171 3 1958 49"18'00" 11456'55" Permian Johnson Canyon 0.6 2.66 13 11 96 SBB86 17J 31957 49'18'00" 114"56'55" Permian Johnson Canyon 0.8 0.67 12 15 84 SBB86 17K 31958 49"18'00" 11456'55 Permian Johnson Canyon 1 2.38 11 12 138 SEE86 17L 3 1959 49"18'00" 114'56'55 Permian Johnson Canyon 0.4 :.33 21 $4 512 SBB86 17M 31960 49"18'00" 114"56'55 Permian Johnson Canyon 1 0.58 13 13 48 SBB86 17N 31961 49"18'00" 114'56'55" Permian Johnson Cnyon 1 1.56 15 13 201 SEE86 t70 31962 49'18'00" 114"56'55" Permian Johnson Canyon 0.8 1.19 18 13 186 SBB86 17P 31963 49"18'00" 11456'55 Permian Johnson Canyon 1 172.52 12 57 SBB86 17Q 31964 49Y8'00" 114'56'55" Permian Johnson Canyon 2 0.49 20 14 336 SBB86 17R 31965 49'1 8'00" 114"56'55 Permian Johnson Canyon 3 0.28 20 15 258 SEE86 17s 31966 49"18'00" 11456'55" Permian Johnson Canyon 0.2 4.58 9 22 80 SBB86 20 31967 49"51'00" 114'43'40" Jurassic Fernie grab 27.4 30 23 48 SEE86 2OA 31968 49'51'00" 114-43'40" Jurassic Fernie 0.3 29.4 29 28 45 SEE86 21A 31969 49"51'55 114"47'10" Permian Johnson Canyon grab 13.8 10 15 183 SEE86 216 31970 49"51'55 114'47'10" Permian Johnson Canyon 0.7 0.7, 8 8 19 SEE86 22449"5220" 31971 114"46'40" Jurassic Fernie 0.55 2.7' 13 32 42 SB B8 6 24 31972 49"1850 31972 24 SBB86 114'55'30'' Fernie 24 Jurassic 19 14.3 0.12 222

'PZOs Analyses done byXRF Error *+AI18 1% Absolute for values Remaining P20~samples analyzed by volumetricmethod Sa m ple Lab Latitude Lab Sample Longitude Age Formation Wldth bo5 cu Pb Zn Number Number (N) (W (metres) (%) (ppm) (ppm)

SBB86 27A 31973 49'06'20" 114"4045" Permian Ranger Canyon 1 1.1. 10 8 18 SBB86 278 31974 49"06'20" 114"40'45 Permian Ranger Canyon 1 1.3' 14 7 33 SBB86 28 31975 49"05'03" 114"39'30" Jurassic Femie 2 13.7 64 22 195 58686 29A 31976 50"07'00" 114'45'30'' Permian ? grab 2.1' 7 15 24 SBB86 30 31977 49"3905 114"44'00" Jurassic Fernie grab 0.4' 13 31 525 SBB86 31A 31978 49"39'10" 114"44'00 Jurassic Fernie 1 23.8 38 20 714 , SBB86 31 B 31979 49"39'10" 114"44'00 Jurassic Femie 1 8.8 35 15 140 SBB86 31C 31980 49"39'10" 114"44'00" Jurassic Fernie 0.6 7.9 32 20 80 SBB86 31D 31981 49"39'10 114"4400 Jurassic Fernie 2 0.4. 46 26 246 SBB86 36A 31982 49-27'30" 114"41'40" Permian Johnston Canyon grab 1.7' 5 8 24 SBB86 37A 31983 49"27'10" 114"41'50 Jurassic Femie 0.8 22.4 45 22 144 SBB86 38A 31984 49"06'40" 114'40'45'' Jurassic Femie 1 18 37 25 204 SBB86 388 31965 49"06'40" 114"40'45" Jurassic Fernie 0.2 2.4. 65 20 585 SBB86 38C 31986 49"06'40" 114"40'45" Jurassic Fernie 0.6 9.99 250 41 1500 SBB86 38D 31987 49-06'40 114'40'45 Jurassic Fernie 1.5 0.3* 73 23 204 SBB86 40A 32346 49'09'30" 114"46'00" Jurassic Femie 1.2 15.7 28 13 134 58886 41A 32347 49"09'00" 114"46'20 Permian Johnston Canyon 1 1.6* 4 10 47 SBB86 416 32348 49'0900" 114046'20 Permian Johnston Canyon 1 0.3' 5 109 65 SBB86 41C 32349 49"0900" 114"46'20" Permian Johnston Canyon 1.5 1.1' 6 9 114 SBB86 41 D 32350 49"09'00" 114'46'20" Permian Johnston Canyon 1.5 1.8* 4 10 140 SBB86 42A 32351 49"0930" 114"46'15 Jurassic Fernie 1 18.4 28 11 91 58686 428 32352 49'0930" 114"46'15 Jurassic Fernie 1 18.6 25 23 62 SBB86 43A 32353 49"05'20" 114'36'05" Jurassic Femie 1 22.2 40 20 175 SBB86 44A 32354 49'05'05" 114"39'20" Jurassic Fernie 1 27.5 31 16 110 58686 47A 32355 49"06'20 114"42'45" Jurassic Fernie 1 9.51 46 14 141 SBB86 478 32356 49'0620" 114"42'45" Jurassic Fernie 1 0.4' 61 16 91 SBB86 47C 32357 49"06'20" 114-42'45 Jurassic Fernie 1 0.4' 62 34 167 SBB86 47D 32358 49'06'20" 114"42'45" Jurassic Fernie 1 0.2' 54 16 189 SBB86 47E 32359 49"06'20 114'42'45" Jurassic Fernie 1 0.4' 59 14 257

'P205 Analyses done by XRF Error * Absolute for values Remaining P20s samples analyzed by volumetric method " I

Sample Lab Longitude Lab Sample Latitude Age Formation Width p205 cu Pb Zn Number Number (N) (W) (metres) (W(ppm) (ppm) (ppm)

SBB86 48A 32360 49"0950' 114"40'45" Jurassic Fernie grab 29.2 41 14 128 SBB86 50A 32361 49'06'45" 114'40'50" Permian Ranger Canyon 1 0.8' 3 8 45 SBB86 52A 32362 49"06'55" 114"40'10" Jurassic Fernie 1 .o 14 30 15 115 SBB86 53 32363 49"05'40" 114"41'00" Jurassic Fernie 0.7 0.2' 72 17 138 SBB86 54A 32364 49-05'45 114'41'00" Jurassic Fernie grab 17.6 37 13 160 SBB86 57A 32365 49-57'45" 114"56'25" Permian Johnston Canyon grab 15.8 27 10 94 ! SBB86 58A 32366 4937'40" 114'56'35 Permian Johnston Canyon 1 15.4 28 10 118 SBB86 588 32367 4957'40" 114"56'35" Permian Johnston Canyon 1 13.1 30 11 118 SBB86 61A 32368 49"41'40" 114'56'10" Permian grab 4.2' 3 8 102 SBB86 62A 32370 50'17'50" 115"02'45" Permian Ranger Canyon 1 1.6. 6 7 216 SBB86 626 32371 50"17'50" 115"02'45" Permian Ross Creek 1 0.8* 5 6 75

SBB86 62C 32372 50'17'50" 115-02'45" Permian Ross Creek 1 0.8' 5 5 50 ~ SBB86 62D 32373 50"17'50" 115"02'45" Permian Ross Creek 1 0.4' 5 7 54 58886 62E 32374 50"17'50" 115'02'45" Permian Ross Creek 1 2' 12 12 261 SBB86 62F 32375 50'17'50" 115"02'45" Permian Ross Creek 1 1.7- 8 10 187 SBB88 62G 32376 50"17'50" 115"02'45" Permian Ross Creek 1 0.8* 9 10 65 58886 621 32369 50Y7'50" 115'02'45 Permian Ranger Canyon grab 25.8 12 9 106 SBB86 63A 32377 50'18'10" 115"02'45" Permian Ranger Canyon 0.5 18.6 9 7 159 SBB86 638 32378 50"18'10" 115"02'45' Permian CanyonRanger 0.3 0.2' 9 5 35 SBB86 636 32379 50'18'10 115'02'45" Permian Rangercanyon 1.3 3.8' 10 23 160 SBB86 63D 32380 50"18'10 115"02'45" Permian Rangercanyon 0.9 3.1. 7 10 30 SBB86 63E 32381 50"18'10 115"02'45" Permian Ranger Canyon 1.25 0.2' 8 10 77 SBB86 63F 32382 50'18'10 115'02'45" Permian Ranger Canyon 1.25 CO.1' 5 6 75 SBB86 63G 32383 50"18'10" 115"02'45" Permian Ranger Canyon 0.9 CO.1' 2 7 50 SBB86 63H 32384 50'18'10 115'02'45" Permian Ranger Canyon 1.3 0.3" 5 9 120 58686 631 32385 50"18'10' 115"02'45" Permian Ranger Canyon 0.9 CO.1' 4 5 86 SBB86 63J 32386 50'18'10 115'02'45" Permian Ranger Canyon 0.7 C0.1" 11 8 183 5888632387 63K 50"18'10" 115"02'45" Permian Ranger Canyon 1 CO.1' 9 8 102 0 SBB86 63L 32388 50"18'10 115'02'45" Permian Ranger Canyon 1.3 CO.1' 10 0 112

*P205Analyses done by XRF Error ++A192 1% Absolute forvalues Remaining P205 samples analyzed by volumetric method S am ple Lab Longitude Lab Sample Latitude Age Formation Width p205 cu Pb Zn Number Number (N) (W) (metres) (%) (ppm) (ppm) (ppm)

SEE86 65A 32389 50Y9'20" 115"02'50" Permian Ranger Canyon 1 3' 8 9 55 SBB86 66A 32390 49"48'05 1 15"03'00" Permian Telford grab 11.4 6 9 19 SBB86 70A 32391 49'58'00" 114"48'10" Jurassic Fernie 1 23.2 73 16 272 SEE86 708 32392 49"58'00" 114"48'10" Jurassic Fernie 1 22.7 50 17 165 SBB86 70C 32393 49"58'00' 114"48'10" Jurassic Fernie 0.9 13.4 53 11 137 SBB86 70D 32394 49"58'00" 114"48'10" Jurassic Fernie 1 5.45 61 14 141 SEE86 70E 32395 49"58'00" 114"48'10" Jurassic Fernie 1 3.56 38 8 144 SBB86 71A 32396 49"39'10" 114"42'30" Permian grab 14.5 6 7 54 SBB86 718 32397 49"39'10" 114"42'30" Permian grab 25.7 5 11 132 SBB86 7% 32398 49-44'25" 115"02'50" Permian Ross Creek 0.9 0.9' 16 10 195 ' SEE86 73A 32399 49"44'20" 115"03'00" Permian Ross Creek grab 0.5' 34 11 428 SBB86 74A 32400 49"3605" 115"04'30" Jurassic Fernie 0.5 21.5 40 11 136 SBB86 76A 32401 49'19'50" 114"57'00" Jurassic Fernie 1 SO.1' 10 20 58 SBB86 76B 32402 4979'50" 114'57'00 Jurassic Fernie 1 <0.1* 10 20 56 SEE86 76C 32403 49-19'50" 114"57'00" Jurassic Fernie 0.3 ec.<= 14 22 59 SBB86 76D 32404 49"19'50" 114"57'00" Jurassic Fernie 1 qo.1. 13 22 60 SBB86 76E 32405 49"19'50" 114'57'00" Jurassic Fernie 1 CO.1' 11 20 60 SB.586 76F 32406 49' 19'50' 114"57'00" Jurassic Fernie 0.8 0.5' 9 20 55 56886 77A 32407 49"37'20" 114"39'30" Mississippian Exshaw 0.5 0.7' 85 22 533 SBB86 TIE 32408 49-37'20" 114'39'30 Mississippian Exshaw 0.9 0.2. 50 18 340 SBB86 77C 32409 49'37'20" 114"39'30" Mississippian Exshaw 0.7 0.9' 24 10 59 SBB86 77D 324 10 49"37'20" 114"39'30 Mississippian Exshaw 0.5 0.8' 30 10 78 SBB86 77E 3241 1 49"37'20" 114"39'30" Mississippian Exshaw 1.5 3.6' 58 12 236 33686 78A 32412 49-51'45" 114"59'50" Permian Ross Creek grab 0.1' 24 12 43 58886 79A 32413 49"51'50" 114'59'55" Permian Johnston Canyon 1.o 21.2 9 12 54 SEE86 798 324 14 49"51'50" 114"59'55" Permian Johnston Canyon 0.5 1.5" 6 12 31 SBB86 BOA 32415 50"01'30" 114"57'30" Permian Ross Creek 0.5 2.9' 41 7 152 56886 808 32416 50"01'30" 114"57'30" Permian Ross Creek 0.4 5.93 13 16 78,

SBB86 83A 32417 49"1030" 114"49'10" Pennsylvanian Kananaskis grab 1.3' 10 10 20 ~ SEE86 84A 324 18 49-1 030' 114"49'05" Permian Johnston Canyon 0.25 40, 6 13 28

56886 848 32419 49Y0'30" 114'49'05" Permian Johnston Canyon 1 3.2' 50 11 133 ~ SBB86 84C 32420 49"10"30" 114"49'05 Permian Johnston Canyon 0.4 11.7 43 14 465 SBB86 84D 32421 49"1030" 114'4905' Permian Johnston Canyon 1 1.1' 103 23 1300 SBB86 85A 32422 49'1000" 114"47'00" Permian Rangercanyon 0.6 9.58 8 10 56 SBB86 86A 32423 49"16'50" 114"47'40 Fernie Jurassic 29.5 grab 32 19 66 SEE86 1A 31768 49'w40" 115'05'30" Jurassic Femk 88 52 6 14 55 37 63 3679 286 SEE86 16 31769 49'30'40" 115'05'30" Jurassic Fernie 87 46 5 4 50 40 67 3452 541 SEE86 1c 31770 49'30'40" 115'05'30' Jurassic Femk 111 51 c5 <6 40 34 58 3293 1227 SEE86 ID 31771 49'30'40' 115'05'30" Jurassic Fernie 112 56 <5 1 42 40 68 3232 713 SEE86 2A 31772 49'31'02" 115'05'00" Permian Ranger Canyon 37 39 <5 4 32 18 28 401 821 SEE86 3A 31773 49'39'15" 114V4'10" Triassic Sulphur Mountain 68 21 cg 6 58 19 29 3035 323 SEE86 38 31 774 49'3915" 114'44'10' Jurassic Fer"* 990 350 31 <6 71 127 77 1460 1440 SEE86 3c 31775 49'3915' 114°44'10" Jurassic Femie 1012 211 6 <8 63 96 86 2434 1357 SEE86 3D 31776 49'39'15 114944'10" Jurassic Fernie 372 63 <5 4 46 44 59 3016 396 SEE86 3E 31777 49'39'15 114'44'10" Jurassic Fer"ie 1164 59 15 C6 139 33 34 1627 556 S0086 4A 31778 49*39'45" 114'42'W Jurassic Fernie 1214 485 32 -3 89 2m 116 1253 929 SEE86 46 31779 49'39'45' 114'42'30' Jurassic Fer"* 1290 946 38 5 94 406 224 939 1398 SEE86 4C 31780 49'39'4s 114°42'30' Jurassic Femie 1293 946 42 2 91 409 222 935 1387 SEE86 40 31781 49'39'45" 114'42'30" Jurassic Fernie 1307 792 45 c6 90 332 205 985 1739 SEE86 4E 31782 49'39'45 114'42'30' Jurassic Fern* 1337 617 50 <6 94 247 126 1248 1135 SEB86 6A 31783 49'5420' 114'50'55" Jurassic Fernk 1170 443 30 5 73 168 84 1283 1071 SEE86 68 31784 49'5420" 114'50'55" Jurassic Fernie 1273 563 35 <6 101 265 172 1082 1208 SEE86 6C 31785 49'5420" 114'50'55" Jurassic Fer"ie 700 125 3 1 60 62 47 1921 382 SEE86 6D 31 786 49'5420" 114'50'55" Jurassic Fernie 1084 118 4 5 56 67 64 19% 457 SEE86 6E 31787 49'54'20" 114'50'55" Jurassic Fernie 782 95 <5 5 50 48 59 2M)l 327 SEE86 6F 31788 49'5420' 114'50'55" Jurassic Fer"k 556 83 <5 <6 42 54 44 1787 484 SEE86 6G 31789 49'5420' 114'50'55" Jurassic Fer"* 401 73 c5 14 45 57 50 1530 436 SEE86 6H 31790 49'54'20' 114'50'55" Jurassic Fernie 528 32 0 <6 107 23 29 1452 314 SEE86 78 31921 49'5320' 114'57'00' Permian Ranger Canyon 51 25 c5 3 14 6 21 1332 86 SEE86 8A 31922 49'27'40' 115'06'30" Permian Johmton Canyon 44 49 3 22 35 38 41 1347 2978 SEE86 88 31923 49'2740' 115'0630" Permian Johmton Canyon 30 64 13 18 53 47 54 2787 227 SEE86 8C 31 924 49'27'40" 115'06'30' Permian Johmton Canyon 23 46 6 17 45 29 44 2717 183 SEE86 8E 31925 49'27'40' 115~0630' Permian Ranger Canyon 43 53 11 7 80 35 52 3135 387 SEE86 8F 31926 49'2T40" 115'06'30' Permian Ranger Canyon 35 41 3 5 79 24 40 3420 613 SEE86 8H 31927 49'2740" 115'05'30' Permian Rangercanyon 53 14 5 6 38 23 24 1502 250 SEE86 8K 31928 49'27'40' 115'0630" Permian Ranger Canyon 163 131 37 10 I74 lo6 45 1548 184 SEE86 8L 31929 49'27'40' 115'06'30' Permian Rangercanyon 58 89 11 9 30 43 45 1441 172 SEE86 9A 31930 49'32'02" 115'04'5S' Permian Ranger Canyon 105 51 2 18 44 28 52 2467 272 SEE86 96 31931 49'32'02" 115'04'55" Permian Ranger Canyon 66 28 -=5 9 41 12 35 1818 214 SEE86 9c 31932 49'32'02" 115'04'55" Permian Ranger Canyon 52 26 3 6 37 10 31 2128 203 SEE86 9D 31933 49'32'02" 1 15'04'55' Permian Ranger Canyon 59 29 1 6 41 27 35 2108 2or SEE86 10A 31934 49'31'40" 115'10'40" Jurassic Fernie 1094 164 18 8 88 81 59 787 433 SEE86 1IA 31935 49'31'50" 115'10'4S Jurassic Fe,"ie 1117 325 21 11 51 121 71 737 371 SEE86 12 31936 49'58'50" 114e4840" Jurassic Fernie 126 11 5 18 21 19 49 1377 306 SEE86 13A 31937 50'1825" 114'56'05" Jurassic FW"k 329 301 19 11 37 115 78 791 683 SEE86 138 31938 50*1825 114'56'05" Jurassic Fer"* 887 390 27 6 52 121 75 865 2473 SEE86 13C 31939 50'1825 114'56'05" Jurassic Fernie 954 524 40 8 78 196 117 1355 7757 SEE86 14A 31940 50'12'00" 115'W'00' Jurassic Femk 709 576 22 9 69 248 167 1772 3944 9.0"' SEE86 148 -1-1 5e-12'00' 115'"' J??rassic FW!* 275 77 6 16 78 54 74 3355 5871 SEE86 14C 31942 50'12'OW 115'WW Jurassic Fernie 275 79 9 17 73 52 67 3318 5687 58886 14D 31943 50"12'00" 115'WW" Jurassic Femie 378 23 4 12 117 16 37 2071 2743 58886 15A 31314 49'16'05" 114'36'00" Jurassic Fernie 523 575 74 13 108 245 186 2012 283 58886 158 31945 49'16'05" 114'36'00" Jurassic Fernie 221 36 20 18 161 36 63 4805 431 58886 15C 31946 49'16'05" 114'36'00" Jurassic Fernie 212 342 33 14 75 138 128 2540 223 568% 150 31947 4916'05" 114'36'00" Jurassic Fernie 616 784 76 19 104 308 196 1429 255 58886 17A 31946 49'18'00" 114'56'55" Permian Johnston Canyon 60 35 4 12 35 23 35 2281 257 58886 178 31949 49'18'00" 114'5655" Permian Johnston Canyon 54 28 2 8 40 17 36 2352 262 SEE86 17C 31950 49'1800" 114'5655" Permian Johnston Canyon €4 27 <5 9 36 15 40 1864 218 58886 17D 31951 49'18'00" 114'5655" Permian Johnston Canyon 62 31 3 7 66 18 33 2968 291 58886 17E 31952 49'18'00" 114'56'55" Permian Johnston Canyon 87 38 6 la 44 34 40 1913 223 58886 17F 31953 49'18'00" 114'56'55" Permian Johnston Canyon 78 35 1 9 55 28 48 2557 270 58886 17G 31954 49'18'00" 114'56'55" Permian Johnston Canyon 65 29 <5 11 70 9 51 2272 223 SEE86 17H 31955 49'18'00" 114'56'55" Permian Johmton Canyon 72 34 5 11 48 27 44 2722 289 58886 171 31956 49'18'00" 114%6'55" Permian Johnston Canyon 95 39 4 10 53 29 66 2873 303 SEE86 17J 31 957 49'18'00" 114'56'55" Permian Johnston Canyon 65 24 4 6 34 11 33 1953 218 56686 17K 31958 4916'00" 114'56'55" Permian Johnston Canyon 85 35 9 8 37 20 28 1762 268 58886 17L 31959 49'16'00" 114'56'55' Permian Johnston Canyon 72 34 13 6 50 30 42 2561 272 SEE86 17M 31960 49'18'00" 114'56'55' Permian Johnston Canyon 61 23 4 0 34 16 26 2048 221 58886 17N 31961 49'18'00" 114'56'55" Permian Johnston Canyon 73 34 2 8 39 19 54 21 E4 233 *' 568% 170 31962 49'1800" 114'5S55' Permian Johmlon Canyon 75 42 7 I, 52 26 47 27% 244 SBB86 17P 31963 49'18'00" 114'56'55" Permian Johnston Canyon 96 43 9 7 48 27 48 2197 390 58886 17Q 31% 49'1800" 114'5655" Permian Johnston Canyon 68 38 4 9 134 25 39 2917 396 58886 17R 31965 49'18'00" 114'5655" Permian Johnston Canyon 62 38 10 10 75 23 39 3561 308 58886 175 31966 49'18'00" 114'5655" Permian Johnston Canyon 92 55 30 16 60 25 60 1900 271 58886 20 31967 49'51'00" 114O43'40" Jurassic Fer& 1315 907 42 1 126 369 239 1298 15057 58886 2OA 31968 114*43'40" F.X"ie 49'51'00" Jurassic 1216 1147 55 14 139 472 293 1183 17534 ~ 58886 21A 31969 49'51'55" 114*47'10" Permian Johnston Canyon 300 a3 99 12 60 66 43 529 236 58886 218 31970 49'51'55" 114-47'10" Permian Johnston Canyon 125 84 2 3 66 €4 41 402 117 58886 22A 31971 49'5220" 114'46'40" Jurassic FW"k 329 120 4 la 44 94 177 2391 919 58886 24 31972 49'18'50 114'55'30" Jurassic Fer"* 241 66 72 9 67 26 32 1408 a74 58886 27A 31973 49'0620" 114'40'45" Permian Ranger Canyon 87 118 6 6 43 79 50 716 921 58886 278 31974 114*4045' 49'06'20" Permian Ranger Canyon 76 138 12 13 56 85 48 1079 100 ~ 58886 28 31975 49'05'03" 114'3930" Jurassic FW"k 413 455 43 14 131 192 163 2733 443 58886 29A 319756 50'07'00" 114'4S30 Permian 7 79 50 4 5 55 45 50 1245 168 58886 30 319757 49'39'05" 114'4400" Jurassic Fernie 174 34 6 13 71 39 a5 3410 257 58886 31A 319758 49'39'10" 114'44'00" Jurassic Fer"ie 1166 520 40 3 79 213 122 1208 4238 58886 318 319759 49'39'10" 114944'00" Jurassic Fernie 914 230 17 14 65 107 aa 2354 WI 56886 31C 319760 49'39'10" 114*44'00" Jurassic Fer"ie 747 142 22 6 63 63 a8 2106 1920 58886 310 319761 49'39'10" 114*4400" Jurassic Fernie 1286 31 15 2 158 33 36 1852 396 58686 36A 319762 49'27'30" 114°41'40 Permian Johnston Canyon 49 95 12 9 95 73 46 349 67 58886 37A 319763 49'2T10" 114'41'50" Jurassic Fernie 781 452 24 9 74 198 135 2181 230 58886 38A 319764 49'06'40" 114'40'45' Jurassic Fernie 602 596 43 15 89 238 149 2049 ta7 58886 388 319765 49'06'40" 114'40'45" Jurassic Fer"* 51 7 153 23 12 154 67 96 3290 610 58886 38c 319766 49'06'40" 114'40'45" Jurassic Fernie 620 513 80 9 31 3 313 359 2591 689 58886 38D 319767 49'06'40" 114'40'45" Jurassic FH"ie 131 51 a 12 159 37 75 3823 453 SEE86 40A 319768 49'0930" 114'4600" Jurassic Fernie 330 453 45 7 93 205 122 2511 323 SEB864IA 319769 49W9'00" 114'46'20" Permian Johmlon Canyon 76 45 17 <6 41 27 42 1812 262 SBB86 418 319770 49'09'00" 114"&20" Permian Johnston Canyon 35 28 12 " I^*-*^",.*",,-" s55ec ?!E ?! "2 . -. .. . . - -. .. ._ .-. . _.,, -. . 05 % 1: 5 57 52 FC ?&!a 2% SBB86 42A 319773 49'0930" 114'46'15" Jurassic Fer"* 512 520 56 13 92 230 151 2481 968 56886 42B 319774 49"09W 114*46'15 Jurassic Fernie 491 534 81 1 95 224 136 2470 528 58686 43A 319775 49'0520" 114'36'05" Jurassic Fer"* 565 859 81 29 108 295 199 1928 840 58886 44A 319776 49'05'05 114'3920" Jurassic Fernie 471 906 86 17 78 413 229 1290 231 SBBffi 47A 319777 49'0620" 114'42'45" Jurassic Fernie 441 197 46 14 97 109 98 2761 439 58886 478 319778 49'0620" 114'42'45" Jurassic Fernie 262 39 29 17 121 27 55 2256 814 319779 58886 47C 319780 49"0620" 114'42'45" Jurassic Fernle 785 46 24 7 148 29 48 1966 356 58886 47D 319781 49'0620" 114'42'45" Jurassic Fernie 1217 29 18 36 194 13 33 1527 448 58886 47E 319782 49'0620" 114'42'45" Jurassic Fernie 1120 37 28 23 211 32 42 1854 684 SBBffi 48A 319783 49'0950" 114°40'45" Jurassic Fer"* 771 793 92 43 117 330 197 1438 182 SBEffi 50A 319784 49'06'15" 114*40'50" Permian RangerCanyan 73 78 22 4 39 69 44 310 69 SEE86 524 319785 49'06'55" 114'40'10" Jurassic Fernie 565 415 48 15 65 193 147 2470 321 SEBffi 53 319786 49'05'40" 114'41'00" Jurassic Fernle 89 30 15 1 280 40 61 4114 275 SBB86 54A 319787 49'05'45 114'41'00" Jurassic Fernie m 515 54 18 106 1 52 1931 437 58886 57A 319788 49'57'45" 114'5625" Permian Johmton Canyon 1028 665 60 21 72 312 179 749 414 sa686 SA 319789 4Y57'40" :y56'35" PermiaR Jch"s!on Canyon 972 784 83 18 92 369 217 717 575 SEE86 588 319790 49'57'40" 114'56'35" Permian Johm!m Canyon 417 487 45 13 72 207 127 1419 279 SBE86 61A 319791 49'41'40" 114'56'10" Permian 107 52 60 2 18 17 31 789 81 58886 62A 319792 50'17'50" 115'02'45" Permian Ranger Canyon 85 67 29 0 87 44 42 647 243 58886 628 319793 50'1750' 115'02'45" Permian ROSS Creek 39 50 16 1 30 32 33 507 113 58886 82C 319794 50'17'50" 115'02'45" Permian Rms Creek 85 44 24 3 50 24 21 6R 834 ' 56886 620 319795 50'17'50" 115"02'45" Permian Rass Creek 44 29 17 10 40 28 38 1688 223 58686 62E 319796 50'17'50" 115'02'45" Permian ROSSCreek 146 44 26 7 60 37 38 2118 2550 58686 62F 319797 50'17'50" 115'02'45" Permian Ross Creek 62 49 26 1 50 45 39 2077 240

La b Sample Lab S F Cd Pb La Ce U Y v Corg CaO R203 N um be r NumberNumber % % (ppm) (ppm) ( ppm ) % p205 pz05

30241 85 21 3 0.34 2.31 14 15 178 40 133 620 1532.21 1.08 0.08 30242 85 21 4 0.33 2.49 10 15 159 40 89 532 87 0.74 2.4 0.1 1 30243 85 23 1 0.08 0.56 3 8 16 40 34 76 76 0.19 1.59 0.33 30244 85 23 3 2.12 0.36 3 12 167 40 63 43 1 59 2.1 0.51 I 0.2 30245 85 23 4 0.28 1.62 1 10 43

A verag e 0.32 1.71 0.32 Average 75 9 20 13 95 337 2.76170 0.89 0.53 APPENDIX 13 MAJOR OXIDES WAPITI LAKE (A. LEGUN, 1985 ) (Values in per cent)

L ab Lab Lab bo5 Si% A1203 Fez03 MgO CaO NazO K20 TiOZ MnO N um be r NumberNumber

30241 8521 3 22.33 8.17 0.560.8 0.39 49.4 0.34 0.350.018 0.09 30242 85 21 4 20.29 9.31 1 0.52 0.64 48.72 0.4 0.40.021 0.08 30243 85 23 1 6.83 76.13 0.88 1.26 0.14 10.87 0.08 0.290.008 0.06 30244 85 23 3 20.3 16.32 2.091.07 1.06 42.82 0.54 0.020.8 0.21 30245 85 23 4 14.81 18.16 2.14 0.82 2.1 1 40.73 0.48 0.840.024 0.18 30246 85 242A 19.79 16.5 1.98 1.24 0.57 43.45 0.54 0.78 0.18 0.018 30247 85 24 28 20.08 11.13 1.11 0.45 1.21 45.96 0.36 0.43 0.1 1 0.014 30248 85 24 2c 3.28 38.46 6.57 3 4.56 18.55 0.62 2.75 0.46 0.027 30249 85 25 1A 17.82 15.28 1.78 0.99 0.93 45.17 0.52 0.66 0.16 0.019 30250 85 25 18 8.24 12.7 1.71 1.26 2.31 44.6 0.23 0.77 0.1 0.029 30251 85 25 2 15.52 10.69 1.04 0.69 0.6 48.32 0.31 0.440.015 0.1 30252 85 26 1 16.22 52.77 0.83 0.79 0.14 25.32 0.13 0.26 %X 0.0% 30253 85 26 2 14.77 16.48 2.04 0.94 2.36 42.51 0.46 0.79 0.13 0.025 30254 85 26 3 20.33 22.15 0.572.9 1.26 38.32 0.67 1.15 0.27 0.033 30255 85 21 3D 22.54 NIA N/AN/A N/A N/A N/A N/ANIA NIA

Average1.27 1.05 1.9216.21 23.16 0.02138.91 0.160.41 0.77

N/A Not analyzed

APPENDIX 14 RESAMPLING RESULTS OF THE ABBY AND HIGHWAY 3 PHOSPHATE LOCALITIES

Sample Lab LongitudeLatitude Fwmation Wath P20, C" Pb zn U V Y la ce so Ntmber Number (N) IW (metres) (%) (ppm) (ppm) (ppm)(ppm) (ppm)(PFN (ppm) (Ppm) (Ppml

SB87 1A 33512 50'18'25" 114'56'05"50'18'25"33512SB871A Femie 0.6 3.81 33 20 14 29 20 14.1 51201 49 SB87IB 50'18'25"114'56'05"33513 Femie 1 22.0513 52 63 27 55 355 47.799 61 SB87 1C 33514 50'18'25" 114'56'05"50'18'25" 33514 SB871C Femie 17.79 0.5 48 18 74 29234 71 55 31 45.1 SB 871D 33515 50'18'25"114'56'0533515SB871D Femie 1 18.3291 44 349 14 33 64 19 60 34.2 SB871 E 33516 50'18'25" 114'56'0550'18'25"33516 SB871E 43 Femie 26.63 0.9 70 17 33 59 484 53.8136 69 SB87 1F 33517 50'18'25" 114'56'05"50'18'25" 33517 SB871F Femie 19 163 0.15 95 15 76 26 18.7s7 41

SB8724 49*3915"114'44'10"33518 73 Femie16 460.7 24.88 46355 82 136 79 52.1 588728 49'3915"33519 114'44'10' Femie 0.5 IW8 15734 17 NE 61 296 228 155 57.7

ND- Notdetermined APPENDIX 15 MAJOR AND TRACE ELEMENT ANALYSES - ALEY CARBONATITE (Values in percent)