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UBC Theses and Dissertations

Hydrothermal alteration and rock geochemistry at the Berg porphyry copper-molybdenum deposit, north-central… Heberlein, David Rudi 1984

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HYDROTHERMAL THE  A L T E R A T I O N . AND  BERG PORPHYRY  ROCK G E O C H E M I S T R Y  COPPER-MOLYBDENUM  NORTH-CENTRAL  BRITISH  AT  DEPOSIT,  COLUMBIA.  by D A V I D RUDI I.Sc,  The U n i v e r s i t y  HEBERLEIN  of. S o u t h a m p t o n , E n g l a n d ,  A T H E S I S SUBMITTED IN P A R T I A L F U L F I L L M E N T THE  REQUIREMENTS MASTER  FOR OF  T H E D E G R E E OF  SCIENCE  in THE  FACULTY  Department  We  accept to  THE  OF GRADUATE  of Geological  this  thesis  the reauired  UNIVERSITY  David  Rudi  Sciences  conforming  standard  OF B R I T I S H  October, 0  as  STUDIES  COLUMBIA  1984  H e b e r l e i n , 1984  1980  OF  In p r e s e n t i n g  t h i s t h e s i s i n p a r t i a l f u l f i l m e n t of  requirements f o r an advanced degree a t the  the  University  o f B r i t i s h Columbia, I agree t h a t the L i b r a r y s h a l l make it  f r e e l y a v a i l a b l e f o r reference  and  study.  I  further  agree t h a t p e r m i s s i o n f o r e x t e n s i v e copying o f t h i s t h e s i s f o r s c h o l a r l y purposes may  be granted by the head o f  department or by h i s o r her  representatives.  my  It is  understood t h a t copying or p u b l i c a t i o n of t h i s t h e s i s f o r f i n a n c i a l gain  s h a l l not be allowed without my  permission.  Department o f The  U n i v e r s i t y of B r i t i s h Columbia  1956  Main M a l l  Vancouver, Canada V6T  1Y3  Date  DE-6  (3/81)  "Tl^H  2%/fgr~  written  Abstract  I n r e c e n t y e a r s our u n d e r s t a n d i n g of the g e n e s i s of porphyry copper systems has advanced  t o a s u f f i c i e n t l e v e l t o be a b l e t o  c o n s t r u c t p r e d i c t i v e models t h a t enhance e x p l o r a t i o n f o r these d e p o s i t s . Our u n d e r s t a n d i n g of p r i m a r y and secondary geochemical d i s p e r s i o n around t h e s e d e p o s i t s i s not so advanced as v a r i a b l e s such as c l i m a t e and topography cause geochemical p a t t e r n s t o be d i s t o r t e d or masked a t s u r f a c e w i t h the r e s u l t of d i f f e r e n t d e p o s i t s h a v i n g q u i t e d i f f e r e n t geochemical c h a r a c t e r i s t i c s . I n t h i s study the geology and g e o c h e m i s t r y of a porphyry copper-molybdenum from the Canadian C o r d i l l e r a i s examined w i t h the aim of d e m o n s t r a t i n g how p r i m a r y g e o c h e m i c a l p a t t e r n s a r e a f f e c t e d by the development  of  a supergene enrichment b l a n k e t and l e a c h e d c a p p i n g . Topographic c o n t r o l s on the e x t e n t of l e a c h i n g and supergene enrichment a r e a l s o explored.  The Berg porphyry copper-molybdenum d e p o s i t i s i n the Tahtsa Mountain Ranges, a p p r o x i m a t e l y 84 km southwest of Houston,  central  B r i t i s h Columbia. M i n e r a l i z e d zones are c e n t e r e d on a c i r c a 50 Ma composite q u a r t z monzonite  s t o c k . Hydrothermal a l t e r a t i o n zones a r e  s i m i l a r t o those of the c l a s s i c model by L o w e l l and  Guilbert.  C e n t r a l zones a r e p o t a s s i c ( o r t h o c l a s e and b i o t i t e ) w h i l e p e r i p h e r a l zones a r e p r o p y l i t i c  ( c h l o r i t e , epidote, carbonate). Intense p h y l l i c  a l t e r a t i o n ( q u a r t z , s e r i c i t e , p y r i t e ) o c c u r s a t the n o r t h and south margins of the s t o c k . Hypogene m i n e r a l i z a t i o n ( c h a r a c t e r i z e d by p y r i t e , c h a l c o p y r i t e and m o l y b d e n i t e ) i s c o n c e n t r a t e d i n an a n n u l a r  zone  s t r a d d l i n g the  localized Telkwa the  deposit.  The  suggests  that  with  quartz  Thirteen the  deposit  collected  specific  of  geochemistry.  the  quartz  spacially  In  diorite  these  i n the  rocks  alteration  was  populations  the  cross  Outcrop hole.  f l a m e AAS  i s solved  and  element  o n t o an  that  binary  alteration  section  Major  of  were  elements  fluorine  used  to  by  study  minerals.  by  field  the  mapping  and  implies  earlier  hornfels ternary  In  zone c o r r e s p o n d i n g  the  that  zone  is  plots  have been added that  to  biotite  hornfels.  p a r t i t i o n e d i n t o a n o m a l o u s and  p r o b a b i l i t y graphs.  a  thought  samples  and  potassium  This  of  been  c u t t i n g r e l a t i o n s h i p s show  stock  zone.  has  of  cross  e x t r a c t i o n was  rocks  side  associated  south  drill  by  school  i t i s an  sampled.  each  east  stock.  north  amounts of  mineralized  annular  a  metals  i t . Major  was  on  to  field  the  rocks  between d i f f e r e n t host  significant  data  with  i n an  the  that  are  hornfelsed  at  aureole  monzonite  hornfelsed  superimposed  Trace metal  suggest  sequential  predates  r e l a t e d to that  A  copper  the  demonstrate  occur  trace  ion electrode.  origin  hornfels  holes  close  rocks  s t u d i e s . One  (GEOLOG) a n d  XRF,  of  a  quartz  where p o s s i b l e by  of  Others  drill  logged  and  Ag  part  grades  altered hornfelsed  i n previous  the  diamond  distribution  The  are  with  were d e t e r m i n e d  the  these  of  Best  a l t e r e d and  nature  diorite.  were  and  Group) v o l c a n i c  they  zone a s s o c i a t e d  diorite  contact.  (Hazelton  f o r much d e b a t e  the  monzonite  i n a l t e r e d quartz  Formation  subject  quartz  hypogene  with  the  background  zone Cu,  Mo  and  mineralogically  defined the  potential  zones.  potassic alteration  peripheral traced and  ore  to  zone. Lead  haloes  around  surface  through  leached  F l u o r i n e i s anomalous over and  zinc  are  orebodies.  an  extensive  supergene enrichment  supergene  sulphide  (covellite,  or  zones can  be  blanket  Sulphides  d e p o s i t but Cu  are  locally  i s hosted  d e p l e t i o n of  interelement  the on  ratios.  tenorite,  dominant host steep  i n the  and  f o r Cu  Enrichment  factors  a)  by  ratioing  supergene values  b)  by  ratioing  to a constant  and  throughout  most  minerals.  be  derived  TiO  ) f o r each  is  with  i n two  to hypogene v a l u e s , o r ,  (e.g.  of  Enrichment  i s demonstrated  can  leached  supergene oxide  oxide  supergene  supergene  n a t i v e Cu)  s l o p e s where  i n carbonate  elements  recognized:  digenite, chalcocite),  (malachite/azurite, cuprite,  developed  of  capping.  supergene m i n e r a l i z a t i o n are  the  These  area  in  potential  zones of  capping.  anomalous  the  Three  oxide  the  ways: '  zone and  then  2  ratioing therefore  this  imply  Results supergene are  between zones.  d e p l e t i o n and  are  >1,  Enrichment enrichment  show t h a t a l l e l e m e n t s  s u l p h i d e and  depleted  elements  value  w h i l e Mo,  oxide Pb  Ag  incorporated into  (ferrimolybdite,  jarosite,  are  In the  goethite  -  iv -  enriched  leached  significantly  immobile  of  (1=hypogene  (studied) are  zones.  and  factors  cap  Cu,  grade).  in Mn  enriched.  l i m o n i t e mineral's  etc.).  <1  the and These  Zn  Acknowledgement  I with  would this  Development  to the Berg  f a c i l i t i e s . Bradshaw stages  to thank  I  and  of  W.K.  the following for their  Limited  property,  would  scope  of  Maggie  E l l i o t t ,  Stanya  and  help  to  financial  and  their  thank  Don  ideas  and  assistance,  analytical Rotherham,  guidance  Peter  during a l l  my  John  wife  Horsky  and  provided  and  Ernie  who  advised  invaluable  me  help  on i n  Leitz  for  their  and,  Milford,  Kim  A.J. Sinclair  3.  i n the laboratory  Matysek,  and  the t h e s i s  2  and  like  C . I . Godwin  Chapters  assistance  f i l e s  for their  publishing  comments  and  study .  Fletcher, and  for providing  data  especially  I a n Thompson  this  direction  Paul  support  thesis:  Placer access  like  Peter  f o r her help  o f t h i s t h e s i s .  -  v  -  Holbek  for their  i n preparing  interesting  the f i n a l  draft  the  TABLE  OF  CONTENTS  Abstract Acknowledgement L i s t of F i g u r e s L i s t of Tables... L i s t of P l a t e s  i  i v viii x x i  CHAPTER 1. I N T R O D U C T I O N 1.1 GENERAL I N T R O D U C T I O N AND SCOPE OF T H E S I S 1.2 STUDY AREA 1.2.1 L o c a t i o n , T o p o g r a p h y and C l i m a t e 1.2.2 P r o p e r t y H i s t o r y 1.2.3 Regional Geology 1.2.4 P r o p e r t y G e o l o g y CHAPTER 2.1 2.2  2.3 2.4  2.5  2 .6 CHAPTER 3.1 3.2  3.3  3.4  1 1 4 '..4 5 7 8  2. HYDROTHERMAL A L T E R A T I O N AND M I N E R A L I Z A T I O N AT THE BERG . DEPOSIT. 11 INTRODUCTION 11 HYPOGENE A L T E R A T I O N . . 12 2.2.1 Petrography of A l t e r a t i o n 13 2.2.1.1 O r t h o c l a s e zone ( I ) . . . 16 2.2.1.2 O r t h o c l a s e - b i o t i t e zone ( I I ) 16 2.2.1.3 B i o t i t e zone ( I I I ) 18 2.2.1.4 P h y l l i c z o n e ( I V ) . . . ' . .......20 2.2.1.5 P r o p y l i t i c zone ( V ) . . . . . . 24 P O T A S S I U M METASOMATISM OF THE TELKWA FORMATION V O L C A N I C ROCKS 25 MINERALIZATION ..30 2.4.1 Ore M i n e r a l i z a t i o n 30 2.4.1.1 Hypogene d i s s e m i n a t e d m i n e r a l i z a t i o n 31 2.4.1.2 Hypogene v e i n m i n e r a l i z a t i o n 32 DISCUSSION • -37 2.5.1 E v e n t s p r i o r t o e m p l a c e m e n t o f B e r g i n t r u s i o n ....... 37 2.5.2 M a g m a t i c h y d r o t h e r m a l p r o c e s s e s 39 2.5.3 A l t e r a t i o n of country rocks 45 2.5.4 T h e r m a l c o l l a p s e 48 CONCLUSIONS '. 50 3. M O D I F I C A T I O N S OF P R I M A R Y G E O C H E M I C A L P A T T E R N S BY L E A C H I N G AND S U P E R G E N E ENRICHMENT 53 INTRODUCTION 53 GEOCHEMICAL A N A L Y S I S 53 3.2.1 Sampling..' 53 3.2.2 S a m p l e P r e p a r a t i o n a n d A n a l y s i s 55 3.2.3 Quality Control 57 RESULTS 57 3.3.1 G e o c h e m i c a l P a t t e r n s i n t h e Hypogene Zone: Major Elements 57 3.3.2 G e o c h e m i c a l P a t t e r n s i n t h e H y p o g e n e Z o n e : T r a c e Elements 59 3.3.3 G e o c h e m i c a l P a t t e r n s i n t h e S u p e r g e n e Zone and L e a c h e d Cap 62 DISCUSSION 67 - v i -  3.5 CHAPTER 4.1 4.2  4.3 4.4  CONCLUSIONS  68  4 . L E A C H I N G AND S U P E R G E N E E N R I C H M E N T INTRODUCTION SUPERGENE ZONATION 4.2.1 Supergene P r o f i l e s 4.2.2 Leaching and O x i d a t i o n I n d i c e s  AT  T H E BERG  DEPOSIT..70 70 72 73 79  DISCUSSION CONCLUSIONS  80 85  REFERENCES APPENDIX APPENDIX APPENDIX  A. B. C.  88 A N A L Y T I C A L METHODS GEOCODER: A l i s t of ANALYTICAL RESULTS  -  symbols  v i i  -  and  codes •  used  i n  94 GEOLOG.10'0 1 1 2  LIST  OF  FIGURES  FIGURE 1.1  PAGE  L o c a t i o n  o'f  the  Berg  porphyry  1.2 L o c a l geology around the Berg i n t r u s i o n s ( c i r c a 50 Ma) crosscut quartz d i o r i t e i n t r u s i o n . . . . . . . 1.3 D e t a i l e d geology showing d i s t r i b u t i o n 2.1  Cross  s e c t i o n s  s h o w i n g ' l i t h o l o g y M0S2  and  ore  of  d e p o s i t . h o r n f e l s  the  Berg  vs_ K ^ O Telkwa  3  Berg quartz monzonite r e l a t e d to an.older 6  deposit  ( F i g ;  i n t e n s i t y ,  1.3:  a l t e r a t i o n  Berg zones  s e c t i o n zonation  deposit 9  A-A ' ) and  Cu ,  abundances  ...17  2.2 Major element t e r n a r y p l o t s that c of the r e g i o n a l Telkwa Formation v o l c a members; f i e l d B: mafic to i n t e r m e d i a t h o r n f e l s e d rocks from the m i n e r a l i z e d 2.3 CaO a l t e r e d zone  deposit  around the m i n e r a l i z e d zone at the of major r o c k units and a l t e r a t i o n  f r a c t u r e  m i n e r a l  copper-molybdenum  p l o t demonstrating Formation v o l c a n i c  ompare the bulk compositions n i c rocks ( f i e l d A: f e l s i c e members) with a l t e r e d and zone ( f i e l d c ) . . 27  potassium enrichment in the rocks from the m i n e r a l i z e d 29  3.1  L o c a t i o n  of  3.2  S e q u e n t i a l  3.3  Major  d r i l l  holes  e x t r a c t i o n  element  sampled  procedure  geochemistry  of  in for  rock  t h i s  study  d r i l l units  core from  54 samples the  ..56  m i n e r a l i z e d  zone . . .  58  3.4 Element zonation in the hypogene, supergene and l e a c h e d capping zones at the Berg d e p o s i t . Element l i n e s represent the d i s t r i b u t i o n of anomalous p o p u l a t i o n s (Tables 3.2 and 3.3) d e f i n e d from p r o b a b i l i t y graphs 61 :  3.5 R e d i s t r i b u t i o n of copper between carbonate, oxide, sulphide and s i l i c a t e m i n e r a l s in the h y p o g e n e s u p e r gene and l e a c h e d cap zones. S t r i p p l o t s d i s p l a y t o t a l , copper (dotted s o l i d l i n e ) , sulphide copper ( s o l i d l i n e ) and o x i d e plus carbonate copper (dotted l i n e ) . Shading o u t l i n e s the supergene enrichment zone 63 4.1 A schematic supergene p r o f i l e i l l u s t r a t i n g the v e r t i c a l d i s t r i b u t i o n of primary and secondary m i n e r a l s . A b b r e v i a t i o n s f o l l o w s : CAP=leached capping, S0X=supergene oxide zone, SUS=supergene sulphide zone, HYP=hypogene z o n e , RSE=residual supergene enrichment zone, ESE=enhanced supergene enrichment C c = c h a l c o c i t e , Cp=chalcopyrite, Cu=native c o p p e r / c u p r i t e , Cv=covel1ite, Dg=digenite, Fm=ferrimolybdite, Gy=gypsum, L i = l i m o n i t e , Mc = m a l a c h i t e / a z u r i t e , P y = p y r i t e , T n = t e n o r i t e . .  are  zone,  4.2 G r a f L o g s t r i p p l o t f o r t h e t o p 175 f t . o f BRG D H 0 7 6 . V e r t i c a l supergene zones.are defined from g e o l o g i c a l data i l l u s t r a t e d at  -  v i i i  -  as  71  l e f t . G - S c a l e s y m b o l s ( A p p e n d i x B) i l l u s t r a t e m i n e r a l a b u n d a n c e s . G e o c h e m i c a l data i s d i s p l a y e d as h i s t o g r a m s a t t h e r i g h t . . . 75 4.3  GrafLog strip  4.4 ' G r a f L o g  strip  plot  f o r t h e t o p 175 f t . o f BRG  plot  f o r BRG  DH080  DH078....  77 78  4.5 A s c h e m a t i c c r o s s s e c t i o n o f t h e B e r g d e p o s i t i l l u s t r a t i n g t h e r e l a t i o n s h i p b e t w e e n s u p e r g e n e z o n e s , w a t e r t a b l e (WT) , g y p s u m l i n e (GL) and t o p o g r a p h y . A r r o w s i n d i c a t e a p p r o x i m a t e p a t h s of ground w a t e r movement f r o m h i l l t o p t o v a l l e y f l o o r 84  - ix -  LIST TABLE  ..  OF  TABLES  •  PAGE  2.1  A l t e r a t i o n  2.2  Vein  3.1  A n a l y t i c a l  3.2  Trace  element  p o p u l a t i o n s :  hopogene  3.3  Trace  element  p o p u l a t i o n s :  supergene  3.4  T i 0  2  r a t i o  data  for  diamond  3.5  T10  2  r a t i o  data  f o r  d i a m o n d . d r i l l  4.1  Leaching  and  f a c i e s ,  a l t e r a t i o n  zones  and  envelope  subzones  at  the  Berg  deposit  m i n e r a l o g y . . .  33  p r e c i s i o n . .  and  o x i d a t i o n  15  57  d r i l l  i n d i c e s  zone  (n=241)  60  (n = 98)  62  zone  hole  BRG  DH085  ...64  hole  BRG  DH085......  ...66  •  80  LIST  OF  PLATES  PLATE 1.1 V i e w o f t h e B e r g d e p o s i t f a c i n g n o r t h . N o t e t h e e l o n g a t e r i d g e t h a t d i v i d e s , t h e c i r q u e i n t o t h e Pump C r e e k ( l e f t ) and Red C r e e k ( r i g h t ) d r a i n a g e s . P o t e n t i a l o r e b o d i e s u n d e r l i e Red C r e e k v a l l e y . 2 1.2 V i e w l o o k i n g s o u t h w e s t a c r o s s t h e d e p o s i t . a t t h e l o w e r r i g h t o f t h e v i e w i s u n d e r l a i n by p o r p h y r y s t o c k (QMP) the l a t e r q u a r t z f e l d s p a r  The p r o m i n e n t ridge the q u a r t z monzonite p o r p h y r y dyke (QFP). 2  2.1 P e r v a s i v e o r t h o c l a s e a l t e r a t i o n ( z o n e I ) o f q u a r t z m o n z o n i t e p o r p h y r y . The p a l e g r o u n d m a s s i s c o m p o s e d o f f i n e g r a i n e d q u a r t z , p i n k o r t h o c l a s e ( O r ) and s e r i c i t e . L a r g e e u h e d r a l b i o t i t e c r y s t a l s are u n a l t e r e d ; pale green p l a g i o c l a s e phenocrysts are p e r v a s i v e l y sericitized 14 2.2 O r t h o c l a s e z o n e ( z o n e I ) a l t e r a t i o n i n q u a r t z m o n z o n i t e porphyry ( c r o s s e d n i c o l s ; s c a l e b a r i s 1 mm). P h e n o c r y s t s of i g n e o u s b i o t i t e ( B i ) i s m a n t l e d by s e c o n d a r y h y d r o t h e r m a l o r t h a c l a s e ( O r ) , l o c a l l y m a r k e d by C a r l e s b a d t w i n n i n g ( c e n t e r o f v i e w ) . P h e n o c r y s t a t t h e t o p r i g h t i s q u a r t z ( Q z ) ^ The g r o u n d m a s s i s a m o s a i c o f q u a r t z , o r t h o c l a s e , . b i o t i t e , s e r i c i t e and opaque m i n e r a l s . . 14 2.3 O r t h o c l a s e - b i o t i t e z o n e ( z o n e I I ) a l t e r a t i o n o f p l a g i o c l a s e b i o t i t e p o r p h y r y . Note t h a t f i n e g r a i n e d h y d r o t h e r m a l b i o t i t e i s p e r v a s i v e throughout the a l t e r a t i o n envelope around a type l a m i c r o v e i n . Type l b v e i n s c u t t h i s e a r l i e r a l t e r a t i o n  .19  2.4 O r t h o c l a s e b i o t i t e s u b z o n e ( z o n e I I ) a l t e r a t i o n i n p l a g i o c l a s e b i o t i t e p o r p h y r y ( p l a n e p o l a r i z e d l i g h t ; s c a l e b a r i s 1 mm). Note p r e f e r e n t i a l r e p l a c e m e n t o f a b i o t i t e p h e n o c r y s t ( B i 1: r e d d i s h b r o w n p l e o c h r o i s m ) by h y d r o t h e r m a l b i o t i t e ( B i 2: o r a n g e - b r o w n p l e o c h r o i s m ) a l o n g c l e a v a g e p l a n e s . The d i s s e m i n a t e d o p a q u e m i n e r a l i s p y r i t e (Py) 19 2.5 B i o t i t e s u b z o n e a l t e r a t i o n ( z o n e I I I ) o f h o r n f e l s e d T e l k w a F o r m a t i o n v o l c a n i c r o c k . Dark c o l o u r w i t h v e i n i n g t h a t d i s p l a y s o n l y weak e n v e l o p e d e v e l o p m e n t ( p o t a s s i c , when p r e s e n t ) i s c h a r a c t e r i s t i c of t h i s z o n e . E q u i l i b r i u m , b e t w e e n v e i n s and p o t a s s i c a l l y a l t e r e d rocks i s implied.. ' 22 2.6 B i o t i t e s u b z o n e a l t e r a t i o n ( z o n e I I I ) i n b i o t i t e h o r n f e l s ( p l a n e p o l a r i z e d l i g h t ; s c a l e b a r i s 1 mm). Note h y d r o t h e r m a l b i o t i t e ( B i 2) o c c u r r i n g a s d a r k f e l t e d m a s s e s a t t h e l e f t a n d c e n t e r o f t h e view 22 2.7 P h y l l i c a l t e r a t i o n ( z o n e I V ) o f q u a r t z m o n z o n i t e A l t e r a t i o n i n t e n s i t y i s r e l a t e d t o a h i g h d e n s i t y of f r a c t u r e s ( c f . Plate 2.8)... 2.8  Phyllic  alteration  (zone  IV)  -  superimposed  xi  -  on  porphyry. vein f i l l e d  highly  23 fractured  h o r n f e l s . T h i s l a t e r s t a g e of a l t e r a t i o n c o l l a p s e of t h e h y d r o t h e r m a l s y s t e m  is  related  to  thermal 23  2.9 Propylitic. alteration ( z o n e V) o f b i o t i t e h o r n f e l s . T h i s d a r k g r e e n r o c k i s s o f t e r and l e s s massive than o r i g i n a l b i o t i t e h o r n f e l s alteration; original hornfelsic t e x t u r e s are p r e s e r v e d . Note the outlines o f v o l c a n i c f r a g m e n t s ( d o t t e d o u t l i n e s ) . The v e i n at the t o p o f t h e s a m p l e i s a l a t e t y p e 3b c a r b o n a t e - c h l o r i t e - s p h a l e r i t e . vein 35 2.10 Green p r o p y l i t i c a l t e r a t i o n ( z o n e V) o f T e l k w a F o r m a t i o n v o l c a n i c f r a g m e n t a l r o c k . O r i g i n a l t e x t u r e s are c l e a r l y v i s i b l e . L i t h i c f r a g m e n t s a r e r e p l a c e d by c o a r s e e p i d o t e and r i m m e d by fine g r a i n e d e p i d o t e and c h l o r i t e . G r o u n d m a s s has a t r a c h y t i c texture..35 2.11 R e t r o g r a d e p r o p y l i t i z a t i o n of q u a r t z m o n z o n i t e p o r p h y r y ( c r o s s e d n i c o l s ; s c a l e b a r i s 1 mm). Igneous b i o t i t e ( B i ) , p a r t i a l l y enclosed i n q u a r t z (Qz), h a s b e e n p s e u d o m o r p h e d by i r o n r i c h c h l o r i t e ( C I ) . N o t e a l s o t h e i n t e n s e c l o u d i n g of plagioclase p h e n o c r y s t s ( P f ) by f i n e s e r i c i t e a t b o t t o m of v i e w 36 2.12 R e t r o g r a d e p r o p y l i t i z a t i o n of p l a g i o c l a s e b i o t i t e p o r p h y r y (plane polarized l i g h t ; s c a l e b a r i s 1 mm). Sericitized plagioclase (Pf) i s replaced'by i r o n r i c h epidote (Ep). A biotite (Bi) p h e n o c r y s t a t t h e b o t t o m l e f t o f t h e v i e w h a s b e e n r e p l a c e d by iron rich chlorite. ..36 P l a t e 4.1 V i e w t o w a r d s t h e h e a d w a t e r s o f Red C r e e k . Note s t r o n g l y d e v e l o p e d g o s s a n ; y e l l o w a r e a s a r e j a r o s i t i c and the p o t e n t i a l o r e b o d y . A c t i v e p r e c i p i t a t i o n of f e r r i c r e t e s beds i n d i c a t e s t h a t l e a c h i n g p r o c e s s e s are a c t i v e today  the overlie in creek 86  CHAPTER  1.1 GENERAL  The  Berg  example copper  INTRODUCTION  porphyry  of a w e l l system  proposed between  rock  documented  recently  by P l a c e r  (1976) d e s c r i b e d  elements  display  a crude  A north this and  study mineral  Panteleyev deposit. of  and  south  cross  that  zones'. T h i s and produce  Primary  an i m p r o v e d  samples) to the surface supergene  demonstrate  whether  'fingerprint' leached  enrichment  terrain.  model  type  Topographic  types  was s e l e c t e d f o r  a l l rock  through  a well  t h e work o f  studied  would  the aim  (from  leached  approach  geochemical  ofthe  with  elements  developed  The a i m o f t h i s  i s  whole cap  to  s i g n a t u r e or  remain  i n a highly  e f f e c t s on t h e i n t e n s i t y o f  - 1.-  alteration  f o rthe formation  are also  of deposit  types,  upon  of c e r t a i n trace  a characteristic  f o rt h i s  that  and a l t e r a t i o n  out to build  patterns  zone.  and showed  of the property  sets  the persistence  a n d more  the deposit.  i tt r a n s e c t s  study  geochemical  overall  d i f f e r e n t rock  about  d r i l l i n g and  A Ph.D t h e s i s i n 1 9 7 6 by  the deposit  section  on t h e b a s i s  documenting  rock  zonation  are well  (Western) Limited  Limited.  i n p y r i t e s from  zones  of e x p l o r a t i o n  Explorations  Development  model  Spatial relationships  and a l t e r e d  years  i s an e x c e l l e n t  to the c l a s s i c  (1970).  and m i n e r a l i z e d  by K e n n c o  deposit  c a l k - a l k a l i n e porphyry  similarities  a s a r e s u l t o f many  mapping  minor  undeformed  and G u i l b e r t  units  property  Panteleyev  copper-molybdenum  close  by L o w e l l  INTRODUCTION  AND SCOPE O F ' T H E S I S  exposed,  with  1  P l a t e 1.1 View of the B e r g d e p o s i t l o o k i n g n o r t h . Note the e l o n g a t e c e n t r a l r i d g e t h a t d i v i d e s t h e c i r q u e i n t o Pump C r e e k ( l e f t ) and Red C r e e k ( r i g h t ) . P o t e n t i a l o r e b o d i e s u n d e r l i e t h e Red C r e e k v a l l e y .  P l a t e 1.2 V i e w l o o k i n g s o u t h w e s t a c r o s s t h e d e p o s i t . The prominent r i d g e a t t h e l o w e r r i g h t o f t h e v i e w i s u n d e r l a i n by t h e quartz m o n z o n i t e p o r p h y r y s t o c k (QMP) and t h e l a t e r q u a r t z feldspar p o r p h y r y dyke (QFP).  -  2  -  Figure  1.1  Location  of  the Berg  -  porphyry  3  -  copper-molybdenum  deposit.  leaching  and supergene  Chapters appearing 1984); 19  2, 3 a n d 4 w e r e  i n Economic  Chapter  (Heberlein  titled  enrichment  are also  prepared  Geology,  79 ( H e b e r l e i n  of Geochemical  e t a l . , 1983) and C h a p t e r  (Godwin  of' E x p l o r a t i o n  et a l . ,  Geochemists  Chapter  Design"  2  and Godwin,  Exploration,  4 as p a r t  " G e o c h e m i c a l ' E x p l o r a t i o n Program  Association  N  forpublication:  volume  3 i n the Journal  explo red.  volume  of a short  course  given at the  Symposium,  Reno, 1984  1984)  1.2 STUDY AREA  1.2.1  Location,  The of  Berg  central  British  British  (Plate  drains  west  tertiary south. talus bury of  copper-molybdenum d e p o s i t i n t h e T a h t s a Ranges o o C o l u m b i a ( 5 3 4 9 ' n o r t h ; 127 22' w e s t ) , i s  84 km s o u t h w e s t  Mineralized bowl  Columbia  zones  of Houston  (Fig.  1.1) on .the n o r t h e a s t f l a n k into  Bergeland  Local covered  t h e main  valley  C r e e k i n the  Creek  elevations  floor  (Plate  un d e r 1 i e of  a cirque  a g l ac i a ted  C r e e k , The c i r que i s d i v i d e d  (Plate  b u t hav e been 1.2 a n d F i g u r e  -  4 -  like  v a i l ey  that  i n t o two  nor th  slopes are moderately steep at lower  a n d 585 km n o r t h o f  1.1).  at the Berg deposit  d r a i n a g e s ; Pump  Bergeland  and C l i m a t e  porphyry  approximately Vancouver,  Topography  a n d Red C r e e k i n t h e o o (20 t o 30 ) and are 1.1). G l a c i a l  incised  t i l l  deposits  by t h e n o r t h  1.3). Outcrop  fork  i s limited  to  r i d g e  c r e s t s  e l e v a t i o n s 1,200  i t  m with  Climate w i n t e r s to  t h i s The  a  and  time summer  f r e q u e n t .  maximum  the  is  small  creeks  dry  1.2.2  P r o p e r t y  a f t e r  is  periods  anomaly Kennco program  dry ,  but  runoff  months  and  e a r l y  heavy  w i t h  surface  f a l l  reaches  long  cold  ( l a t e  September  snowbound;  strong  March  to  storms  sudden  r a i n  the  winds.  June.  spring  r a p i d l y  lower  Spring  During  are  common.  storms  are  d i m i n i s h e s  and  most  up.  were  d i s c o v e r e d  1948  the  staked The  Lead  in'  of  1967 ;  E x p l o r a t i o n s ,  f i r s t near  for  copper i t s  and  syndicate  molybdenum gossan  P a n t e l e y e v ,  1976  L i m i t e d  d i s c o v e r e d  an  - 5 -  the  e a r l y  To  the  copper  that  now  deposit  form  was  and  1981).  e x t e n s i v e  1920's had  been  part  of  the  f i r s t  a s s o c i a t e d  an  late  c l a i m s ,  and  s t a r t e d  1900's  showings  r e l o c a t e d  l e a d - s i l v e r ,  l a r g e  in  Mountain.  g o l d - t u n g s t e n  (Western)  e v e n t u a l l y  prospected  S i b o l a  Empire  1929  Berg  v i r t u e  (Stewart,  that  snow  by  surface  In  by  the  through  r e l a t i v e l y  staked.  recognized  and  heavy  Ranges  was  p r o p e r t y .  w i n t e r  r e l i e f  at  Ney).  v a r i a b l e  the  to  L o c a l  (Mt.  In  s u b j e c t  l e a d - z i n c - s i l v e r ,  Berg  very  f r o z e n  s e v e r a l  o r i g i n a l l y  is  m  while  H i s t o r y  Tahtsa  gold  2,700  is  enhanced  e l e v a t i o n s ,  channels.  of  ground  season dry  Ranges  proceeds  higher  creek  summers.  f l o o d s  In  The  Tahtsa  thawing  f l a s h  to  at  e l e v a t i o n  warm  the  region  g u l l i e s  r e s t r i c t e d  short  May)  short  runoff  is  of  and  e a r l y  e n t i r e is  and  geochemical  Subsequently e x p l o r a t i o n  supergene  enrichment  LEGEND Intrusive Breccia Berg Quartz Monzonite Quartz Diorite Skeena Gp. Clastic Rocks Skeena Gp. Volcanic Rocks Hazelton Gp. Volcanic Rocks Hornfels Limit of Cu-Mo Mineralizatior Dike Fault Geologic Contact  1km SCALE  f i g u r e i . z L o c a l g e o l o g y a r o u n d cne d e r g m o n z o n i t e i n t r u s i o n s ( c i r c a 50 Ma) c r o s s older quartz d i o r i t e i n t r u s i o n .  -  6  -  a e p o s i t . tserg q u a r t z c u t h o r n f e l s r e l a t e d t o an  blanket  over  Drilling  to  copper  and  1980  Development  Eocene  1981;  Woodsworth,  rocks  that  tuff are  are a  and  of  flow  1981:  flow  by  pinch  work by  0.348%  cutoff;  has  involved  Placer  i n the  green,  grey,  a  area  1981). of  and  with  quartz  Group and  rocks  basalts.  East  are  the  (Carter,  Berg  maroon  the  1974,  Group  deposit  lithic  Skeena  diorite  Middle  intrude  Hazelton  tuffs,  Group  intrusion  of  the  n o r t h . These  siltstones  that  with  is relatively  -  7  of  the  distinguish  out  the  typically  Many  .rocks  area  i n the  that  to  1.2).  units.  and  ( F i g . 1.2)  red  Contacts by  several Early  vicinity  tex.tures that  to  of  rocks  i n the  intruded  Fig.  one  sedimentary  sandstones  Structure  of  equivalent  Recent  Panteleyev,  units.  andesi'tes  Group  and  grained  exposed  trachytoidal  dominated  units  Cu  testing  stocks  Group  1980;  o v e r l y i n g Skeena  Hazelton is  well  on  porphyry  1979,  sequence  vesicular  exhibit  metallurgical  Skeena  everywhere  (Panteleyev,  The  tonnes  million  ( w i t h a 0.25%  i s centered  and  b r e c c i a s and almost  308  communication).  and  monzonite  Hazelton  of  of  mineralization.  Geology  deposit  quartz  consist  reserves  molybdenite  Ltd.  Berg  Mesozoic  personal  drilling  Regional  The  confirmed  1983,  diamond  1.2.3  c h a l c o p y r i t e and  0.052% m o l y b d e n i t e  Rotherham, more  hypogene  rocks rare  simple.  -  flow  them  property overlie  amygdaloidal  the the  are  units  from  Skeena lower  fine  to  conglomeratic Poorly  the Group  volcanic medium horizons.  developed  open  folds  with  to  degrees.  30  regional  1.2.4  area  Stewart  the  rock  viewpoint that  rocks  of  volcanic  rocks  and  steeply  dipping  contact  dips  monzonite  latter rocks  to  outcrops steeply  (QPP)  the  mafic  cause  dikes  local  dips  follow this  a  quartz on  of  10  general  northwards  Group.  the  west  and  400  towards  patterns  stock  flank  quartz  the  metres the  the  700  are the  -  and  m  altered  regular stock  An  the  and  where the  the quartz  porphyry  of  style  (QFP).  altered  intrusive  monzonite  of  an  Formation  comprise  south  classic  a core  8  approximately  f e l d s p a r porphyry  stock.  to  f o l l o w the  -  from  a quartz plagioclase  phases  quartz  G u i l b e r t (1970) w i t h  significant  between' the  phases  (QMP),  monzonite of  of  described  1981).  plagioclase biotite  porphyry  south  stock  Contacts  intrusive  grained  most  first  h o r n f e l s e d Telkwa  monzonite  Four  a l l other  north  alters  was  (1976,  The  monzonite  porphyritic  approximately  and  present.  Hazelton  the  ( F i g . 1.3)  Panteleyev  quartz  monzonite  cuts  by  are  a coarse  and  Alteration Lowell  is a  shallowly).  quartz  the  types  (except  stock:  unit  later  i n t r u d e s and  volcanic  porphyry  and  trends  m i n e r a l i z e d zone  ( 1 9 6 7 ) and  diameter  a  faults  axial  Geology  of  major  economic  (PBP),  northeast  trend  Five  in  to  Normal  Property  The by  north  the  volcanic  breccia  stock  and  contact.  proposed  potassic  The  by  alteration  dips  LEGEND Rock Units  Alteration Zones  Intrusive Breccia  Quartz Diorite  Quartz Monzonite Porphyry  Altered Hornfelsed Tdkwa Fm.  Quarrz Plagioclase Porphyry  I  Ptogioclase Biotite Porphyry  Quartz Feldspar Porphyry  1  J  H  Hornfelsed Telkwa Fm.  K F - Qz  11  KF-Bi  Ill  Bi  potassic  IV  Qz-Se  phyllic  V  CI - Ep  propylitic  F i g u r e 1.3 D e t a i l e d g e o l o g y a r o u n d t h e m i n e r a l i z e d z o n e a t t h e B e r g d e p o s i t showing d i s t r i b u t i o n o f major rock u n i t s and a l t e r a t i o n zones.  -  9  -  (orthoclase zone  quartz limit  Sulphide  monzonite  copper  the  of  potential quartz  volcanic  Supergene are that  being  "limonite"  gossan.  supergene  waters.  (jarosite  rich  hematite  1981)  This  close  area  potential  rich  An  and  also zone.  ore  occur  quartz  to  extends  the  corresponds  over  by  and  pyrite  dominantly  diorite  and  the  the  outer principle  i s accompanied halo  surrounds  as  as  from  altered  with  with  zone  1 km  C h a l c o p y r i t e i s the  zone  extensive  Sulphides  by  minor  the  disseminations  veins  in  in  the  rocks.  processes  after  that  phyllic  propylitic  contact  oxidized in a  remain  calcite)  extensive  1976,  i n the  zone.  an  thin  i s hosted  stock.  monzonite  hornfelsed  and  and  a  mineralization primarily  molybdenite. ore  s u c c e s s i v e l y by  pyrite)  potassic alteration  mineral  amounts  and  (Panteleyev,  of  surrounded  epidote , a l b i t e  deposit.  hornfels  the  biotite)  (quartz, -sericite  (chlorite, the  and  are zone  still of  o x i d a t i o n of Thick  active  l i m o n i t e ) to  the  colour brown  sulphides  10  form  v a r i e s from or  -  Primary  surface.  platforms  limonite).  -  Berg.  l e a c h i n g near  ferricrete  Limonite  at  red-brown  mark  a  sulphides  Iron  oxides  distinctive emergence  orange-yellow (goethite  and  of  2 HYDRO-THERMAL A L T E R A T I O N  CHAPTER  AND  MINERALIZATION  AT  THE  BERG  DEPOSIT  2.1  INTRODUCTION.  Previous zonation  of  monzonite  northeast  ore in  zone  on  and  the  Early  a  of  stock  r e f i n e d the  biotitic implied with  that  geology  diorite quartz  then  origin  major  metasomatism  of  term  Howard,  potential  the at  deposit the  of  in  ore  quartz,  1973)  zones;  to  contact  'biotite  this  the  contact  side  of  the  zone  i s of  of  (1967)  associated 1981)  hydrothermal  proposed  altered after  deposit  these  (1976,  metamorphosed  that  "biotitic  origin  Panteleyev  by  that the  origin, these  quartz  emplacement  of  the  stock.  the  biotitic  analyses  occurred  and  rocks  to  demonstrate  that  -  i s resolved  the  11. -  rocks  that have  of  Panteleyev  s t u d i e s . Stewart thermal  a  recognized  origin  h o r n f e l s ' and  thermally  and  within  The  these  stock.  of  east  zones  diorite".  Berg  part  first  of  shaped  hydrothermally  element has  the  least  been  monzonite  The using  the  have and  at  of  are  1967;  consistent  central  situated close  abundant  resolved  rocks  the  a  potassically. altered rocks.  quartz  not  these  that  retained may  was  intrusion  suggested  rocks  "biotitic  rocks  the  zone  fractured, crescent and  distict  identified  about  (Stewart,  two  in  has  minerals  southeast  m i n e r a l i z a t i o n i s most highly  deposit  studies  presence and  Berg  alteration  monzonite  1981)  hornfels"  but  the  quartz  (1976,  ore  stock.  recognized  the  work  in this  chapter  potassium been  hydrothermally using  data  evolution spatial  2.2  col-lected  Hydrothermal a l t e r a t i o n  during  of the Berg  t h e summer  deposit  argillic this  mineral can  of p e r v a s i v e  assemblages  o f 1980 and a model  i s proposed  study  each  mineral  f o r the  to e x p l a i n observed  zones.  mineralogical subzones  described  minerals.  i s subdivided each  variations.  These  as d i s s e m i n a t i o n s  also  a r e named  after  adjacent  their  monzonite  stock,  to the i n t r u s i o n .  alteration  facies  intrusion.  The o r t h o c l a s e  I I ) occur  based  1970). on  i t s dominant  the p o t a s s i c a l t e r a t i o n  a r e e s t a b l i s h e d on facies,  (Table  mineral  i n the f i e l d however,  In Figure  2.1: zones  (Table  zones  -  12 -  that  2 . 2 ) . The  latter  species.  f o r up t o 1,000 m  i t i s developed best i n 1.3, a p l a n  of t h e d e p o s i t ,  I t o V) a r e c e n t e r e d  monzonite  and  zones and  on t h e  and t h e o r t h o c l a s e - b i o t i t e z o n e s  w i t h i n the quartz  facies  detailed  ore mineral  and i n v e i n s  dominant  c a n be i d e n t i f i e d  the quartz  zones  named a f t e r  2.1) a r e d i s t i n g u i s h e d f r o m  sulphides  from  into  alteration  host  Alteration  phyllic,  the orthoclase, o r t h o c l a s e - b i o t i t e ,  A d d i t i o n a l subzones  (Table  potassic ,  and G u i l b e r t , 1970; R o s e ,  assemblages,  into  a r e c h a r a c t e r i z e d by  w e l l by t h e t e r m s  (Lowell  facies  alteration  component(s) . For example,  be s u b d i v i d e d  biotite  hypogene  and p r o p y l i t i c  consistent  and  are redefined  HYPOGENE A L T E R A T I O N  mineral  and  zones  and t e m p o r a l r e l a t i o n s h i p s o f o r e and a l t e r a t i o n  Facies  In  altered.  (zones I  p o r p h y r y and p l a g i o c l a s e  biotite to  and o u t s i d e  Telkwa IV)  porphyry;  the b i o t i t e  the quartz  Formation  contacts  broad  halo  extending  Zones  fracture  intensity  by  locally  kaolinite  spatial  which  from  processes  and/or  contacts  montmori1lonite of t h i s  alteration  Weak  zones  monzonite  alteration  type  (zone  V) f o r m s  the  a  intrusive  o f maximum are related  argillic  to  alteration  1981) and i s c h a r a c t e r i z e d  with  of f e l d s p a r .  Close  p y r i t i c zones at  and q u a r t z  the a r g i l l i z a t i o n i s probably this  (zone  later,  replacement  alteration  of quartz  alteration  s t r a d d l e t h e n o r t h and  g e n e r a l l y c h a r a c t e r i z e d by p h y l l i c  that  Consequently,  at the Berg.  adjacent  hornfelsed  5 0 0 m t o 1,000 m f r o m  ( F i g . 10 i n P a n t e l e y e v ,  a r e more  indicates  about  Phyllic  that  ( F i g . 2.1) a n d , as shown  association  fractured  diorite. zones  occurs  i n altered,  I I , I I I and IV c o i n c i d e w i t h  ore-forming  occurs  to discontinuous  I I I )mainly  stock  of the s t o c k . P r o p y l i t i c  contact.  the  (zone  monzonite  and i n t h e q u a r t z  i s restricted  south  zone  diorite  intrusions  alteration,  supergene  i s not discussed  in origin.  further  i n this  paper .  2.2.1  Petrography  Mineralogic below,  of  details  i n the order  slightly  Alteration  different  of the a l t e r a t i o n  of t h e i r from  their  sequence spatial  -  1 3  -  zones  are described,  ( I t o V) i n T a b l e distribution  2.1. T h i s i s  outward  from t h e  P l a t e 2.1 P e r v a s i v e o r t h o c l a s e a l t e r a t i o n ( z o n e I ) of q u a r t z m o n z o n i t e p o r p h y r y . The p a l e g r o u n d m a s s i s c o m p o s e d o f f i n e g r a i n e d q u a r t z , p i n k o r t h o c l a s e ( O r ) and s e r i c i t e . L a r g e euhedral b i o t i t e c r y s t a l s are u n a l t e r e d ; pale green p l a g i o c l a s e phenocrysts are p e r v a s i v e l y sericitized.  P l a t e 2.2 O r t h o c l a s e zone (zone I ) a l t e r a t i o n i n quartz monzonite porphyry (crossed n i c o l s ; s c a l e b a r i s 1 mm). P h e n o c r y s t s o f i g n e o u s b i o t i t e ( B i ) a r e m a n t l e d by s e c o n d a r y h y d r o t h e r m a l o r t h o c l a s e ( O r ) , l o c a l l y m a r k e d by C a r l e s b a d t w i n n i n g ( c e n t e r o f v i e w ) . Phenocryst at the top r i g h t i s q u a r t z ( Q z ) . The g r o u n d m a s s i s a m o s a i c of q u a r t z , o r t h o c l a s e , b i o t i t e , s e r i c i t e and opaque minerals . -  14 -  TABLE 2.1. A l t e r a t i o n Facies  Facies,  Zone ^ -  zones  and s u b z o n e s  2  Subzone  P0T 0rthoclase (I) POT O r t h o c l a s e - B i o t i t e ( I I ) POT B i o t i t e (III)  Mineralogy  3  PHY  Quartz-Sericite  PRO PRO  Transition Chlorite-Epidote  ARG  at the Berg Deposit  Biotite-Anhydrite  Or , M s , B i , M g , C p ,Mo Or , B i , A h , M s , M g ,Py ,Cp B i ,Ah,Py,Cp,Mo ,Tz ,F1 Ms ,Py,He,Ka,Mm  (IV) (V) B i o t i t e - C h l o r i t e (V) •  Bi ,Cl,Py,Cp,Cb C I , E p , A b , C b , P y ,Mg ,G1, SI Ka ,Mm,Py  1. Roman n u m e r a l s r e f e r t o a l t e r a t i o n z o n e s on F i g u r e 2.1 2. M i n e r a l a r e i n o r d e r o f a b u n d a n c e a n d a r e c o d e d a s f o l l o w s : Ab=albite, Ah=anhydrite, Cb=carbonate, Cl=chlorite, Cp=chalcopyrite, Ep=epidote, F l = f l u o r i t e , Gl=galena, He=hematite, K a = k a o 1 i n i t e , Mg=magnetite, Mm=montmorillonite, Ms=muscovite ( s e r i c i t i c ) , Mo=molybdenite, O r = o r t h o c l a s e , Py=pyrite, Qz=quartz, S l = s p h a l e r i t e , Tz=topaz. Quartz i s ubiquitous to a l l zones. 3. P O T = p o t a s s i c , P H Y = p h y l l i c , P R O = p r o p y l i t i c a n d A R G = a r g i l l i e . 4. The a r g i l l i c k a o l i n i t e z o n e p r o b a b l y i s o f s u p e r g e n e o r i g i n .  center  of  the  deposit  (Fig.  2.2.1.1 O r t h o c l a s e typified  by  (Plate  2.1)  (Figs.  1.3  original  a pink and and  characteristic;  2.2).  In  grained felted  this  along  that  of  biotite  is a  crystals  primary  vuggy  this  zone  veinlets rutile  and  are  secondary  of  due  quartz  section a  fine  grained  orthoclase, quartz orthoclase also  as  by  planes  is replaced  replaced  chocolate  by  in vein  quartz 1%),  disseminations.  u b i q u i t o u s . These chlorite  by  reddish of  felted  colour  zone,  mainly  Secondary minerals where  and  are  is  alteration  only  closely  latter  but biotite  in thin  section. euhedral  as - f i l l i n g s though  not  chalcopyrite that magnetite,  the  biotite  o c c u r r i n g as  envelopes  fine  grained,  secondary  veins. Sulphides,  are  fine  ( c f . P l a t e 2.4),  brown  orthoclase  groundmass,  or  occur  is  clouded  cleavage  than  sericite  plagioclase is invariably  show s i g n s  (less  and  of  (Plate  crystals  in early  replacement  biotite  Primary  pale  porphyry  and  biotite.  and  is  orthoclase flooding  monzonite  secondary coarser  to  feldspar phenocrysts  i s completely  biotite  rock  hornblende  i s common i n t h e  cavities  the  orthoclase alteration  Igneous  distinctive  i n the  the  secondary  pre-existing  replaced;  Anhydrite  in  of  grain boundaries  matrix  thin  to  a mosaic  rims  sericite.  variably  In  by  zone  masses  ( I ) : Pervasive  c o l o u r a t i o n of  2.1).  on  zone  is restricted  minerals  overgrowths  1.3).  of  abundant  occurs  ilmenite intergrown  as  and with  replace  primary  mafic  type  alteration  minerals .  2.2.1.2 O r t h o c l a s e - b i o t i t e zone (Table  2.1)  i s best  developed  ( I I ) : This  i n the  -  16  -  of  plagioclase biotite  porphyry  F i g u r e 2.1 C r o s s s e c t i o n s o f t h e B e r g d e p o s i t ( F i g . 1.3: s e c t i o n A-A') s h o w i n g l i t h o l o g y , f r a c t u r e i n t e n s i t y , a l t e r a t i o n z o n a t i o n C u , MoS_ and o r e m i n e r a l abundances.  -  17  -  and  (Figs.  1.3  and  sporadically (Plate the  2.3)  2.1),  i n the  from  similar  primary, b i o t i t e  In  thin  biotite  (Plate  section  after  ranges  from  to  orthoclase  veins  5  orthoclase average  zone  3:1  alteration  (less  (Fig.  (Table  composition. basaltic  minerals  2.1)  subzones  dark  hydrothermal  specimen  brown  c o l o u r a t i o n of  biotite.  o r t h o c l a s e zone  biotite  2.4)  or  rock on  Hydrothermal  also  either  has  replaces  replaced  is distributed  as  as  compared other  to  hand  content  less  1%)  and  pyrite  to  to  and  biotite  that  i s less  is similar  primary  whisps  minerals. Hydrothermal  the  ( I I I ) : The  the  biotite and  Panteleyev,  change  of  by  biotite  i s developed  quartz 'diorite  is controlled  Two  zone  volcanic rocks)  The  to  In hand  1%  in  abundant  around  t h a t of  the than  Type  la  the  chalcopyrite ratios  2.1).  porphyry:  alteration.  tan  found  o c c u r r i n g i n vein envelopes  than  Therefore  f o r the  monzonite  zone  the  Sulphide  2.2.1.3 B i o t i t e  to  of  Orthoclase  2.2).  a  i n the  pre-existing  o r t h o c l a s e zone, (Table  porphyry.  is  2.4).  (Plate  10%  zone.  found  secondary  phenocrysts  alteration  monzonite  grained  that  masses  the  fine  to  felted  in  quartz  similar  i t i s c h a r a c t e r i z e d by  groundmass  biotite  however  to a wall  the  best  biotite  -  of p o t a s s i c  i n rocks  of  more  hornfels (originally  the  quartz  compared  diorite  to  7.5%  1981) . e x h i b i t  biotite rock  zone  zone  outward  andesitic  (13.8%  f o r the  well  mafic  mafic quartz  developed  from  the  orthoclase  composition.  zone,  18  -  extending  outwards  biotite  from  P l a t e 2.3 O r t h o c l a s e - b i o t i t e z o n e ( z o n e I I ) a l t e r a t i o n o f p l a g i o c l a s e b i o t i t e p o r p h y r y . Note t h a t f i n e g r a i n e d h y d r o t h e r m a l b i o t i t e i s p e r v a s i v e throughout the a l t e r a t i o n envelope around a type l a m i c r o v e i n . Type l b v e i n s cut t h i s e a r l i e r alteration.  P l a t e 2.4 O r t h o c l a s e b i o t i t e s u b z o n e ( z o n e I I ) a l t e r a t i o n i n p l a g i o c l a s e b i o t i t e p o r p h y r y ( p l a n e p o l a r i z e d l i g h t ; s c a l e bar i s 1 mm). Note p r e f e r e n t i a l r e p l a c e m e n t of a b i o t i t e p h e n o c r y s t ( B i 1: r e d d i s h b r o w n p l e o c h r o i s m ) by h y d r o t h e r m a l b i o t i t e ( B i 2: o r a n g e - b r o w n p l e o c h r o i s m ) a l o n g c l e a v a g e p l a n e s . The d i s s e m i n a t e d opaque m i n e r a l i s p y r i t e ( P y ) . -  19  -  the  orthoclase  and  the  biotite  disappearance  The  rock  2.5).  yellowish  was  rock  thin to  the  ( P l a t e 2.6).  alteration unique trace  amounts  of of  the  present.  molybdenite  of  around  stock  during  i s most  this  later  topaz  developed  biotite  and  by  Most  occur  with  lesser  significant about  -  20  2:1.  -  that  specimen  biotite  is  envelopes,  1973),  by  imply  more that  Purple  and  i s found  in  to  i n diameter,  in  2 mm  subzone,  presence  (Stewart,  5%  outside  i t is typified  i n hand  by  subzone  in this  i s the  first  i s best  grained  (Howard,  and  in vein 1967).  volume) i n in veins amounts in this  the  is restricted  some q u a r t z - a n h y d r i t e - s u l p h i d e  about  average  zone'  potassic alteration.  rare  and  occurs  F i g . 2.1),  felted  veins  g r a i n s , up  subzone  to  fine  or  Fig.2.1).  and  Here  appearance  immediately  appearance  Quartz  throughout  subzone.  chalcopyrite.ratios  and  occurs  stock.  black  the  rock  fluorite  Pyrite which  the  to  irregular  up  2.1  zone',  the  and  'quartz-topaz  section extremely  this  2.1  of. f i n e ' g r a i n e d  Orthoclase,  ( F i g . 2.1:  biotite-anhydrite are  as  envelopes  feature  abundant  brown  contact  and  of  35%)  i s conspicuous  veins  the  orange-brown.  to  (Table  I t i s v a r i a b l e i n width  to  dark  added  anhydrite quartz  In  brown  common n e a r silica  a  b i o t i t e - a n h y d r i t e subzone  (Table  'biotite  contact  (15  the  minerals  the  contact.  southeastern  the  (Plate  are  i s c h a r a c t e r i z e d by  ( 1 9 6 7 ) as  ( 1 9 8 1 ) as  v a r i a b l e • amounts gives  Each  specific  Stewart  intrusive the  subzone.  of  by  Panteleyev  at  ( F i g . 2.1),  b i o t i t e - a n h y d r i t e subzone  described  •the  zone  to  veins.  envelopes  Sulphides  A of  are  the  but " d i s s e m i n a t i o n s of  chalcopyrite  subzone.  Pyrite  and to  Transition marked  by  the  texturally outlines  outline  zones  are  felted  in this  similar.  subzone  grained  to  nature  chemistry  must  used  thermally  metamorphosed  sulphides  i s the  1:1  of  the  are  be  most  Molybdenite  grades,  decrease  alteration  later  sericitized  particularly Intrusive  at  have  Koski in  metamorphic  been  and  and  reported  Cook,  this  apparent  the  -at  1982).  subzone  hydrothermal  biotite  zone  M i n e r a l o g i c a l l y the  rock  alteration  from  abundance  Pyrite  to  chalcopyrite ratios  than  subzone  of  this  5%  by  not  and  of  over  Due  biotite  feature  reach  the  i t is  associations, textures  ( I V ) : Although  in a  phyllic  b e c o m e more  ( i t contains of  volume..  i n the b i o t i t e - a n h y d r i t e  outwards.  abundant  intense  by  biotite  lower  event  around  that  textures  separate  alteration  envelopes  ghost  groundmass  mineral  potassic  and  subzone  i n the  sulphides  2 . 2 . 1 . 4 P h y l l i c .zone  pyrite  fluorite;  crystals  the  generally  and  biotite  diagnostic  total  topaz  biotite  is  Subparallel  Arizona,  rocks.  F i g . 2.1)  occur.  potential orebodies).  common a n d  subzone,  to  and  textures  d i s t i n g u i s h between therefore  the  fragments  of  petrographically,  In  2.1  and  (similar  deposit,  (Table  of ' a n h y d r i t e ,  secondary  porphyry  fine  possible  both  subzone  pre-existing minerals  of  Christmas the  biotite  pre-existing volcanic  outwards  to  the  disappearance  both  of  alignment  to  occurs  veins  alteration  u n i t s are  throughout  the  characterized  by  from  the  deposit, (Table  early i t is  2.1)  most  quartz,  feldspars, especially plagioclase, in  quartz  the  sericite  north more  that  occurs and  crosscut at  south  strongly  -  21  the  earlier  contact  margins  (Figs.  sericitized  -  of  alteration. the 1.3  stock and  ( P l a t e 2.7)  Most and  2.1). than  P l a t e 2.5 B i o t i t e s u b z o n e a l t e r a t i o n ( z o n e I I I ) o f h o r n f e l s e d T e l k w a F o r m a t i o n v o l c a n i c r o c k . Dark c o l o u r w i t h v e i n i n g that d i s p l a y s o n l y weak e n v e l o p e d e v e l o p m e n t ( p o t a s s i c , when p r e s e n t ) is characteristic o f t h i s z o n e . E q u i l i b r i u m between v e i n s and potassically altered rocks i s implied.  P l a t e 2.6 B i o t i t e s u b z o n e a l t e r a t i o n ( z o n e I I I ) i n b i o t i t e h o r n f e l s ( p l a n e p o l a r i z e d l i g h t ; s c a l e b a r i s 1 mm). N o t e h y d r o t h e r m a l b i o t i t e ( B i 2) o c c u r r i n g a s d a r k f e l t e d m a s s e s l e f t and c e n t e r of t h e v i e w . -  22 -  at the  P l a t e 2.7 P h y l l i c a l t e r a t i o n ( z o n e I V ) o f q u a r t z m o n z o n i t e p o r p h y r y . A l t e r a t i o n i n t e n s i t y i s r e l a t e d to a h i g h d e n s i t y of vein f i l l e d f r a c t u r e s ( c f . P l a t e 2.8).  I fry*".- •i-f^*  . Jf.*'5jj?'  P l a t e 2.8 P h y l l i c a l t e r a t i o n ( z o n e I V ) s u p e r i m p o s e d on h i g h l y f r a c t u r e d h o r n f e l s . T h i s l a t e r s t a g e of a l t e r a t i o n i s r e l a t e d t h e r m a l c o l l a p s e of the h y d r o t h e r m a l system. -  23  -  to  altered, is  hornfelsed  t h e main  alteration. relatively per  Thus  factor  i n the center  unfractured  v e i n s . Towards  densities  t o t a l l y replaced  the  stock  that  the o r i g i n a l  soft,  pale  chalky  around  quartz  Other  montmorillonite,  than  where  (quartz  rock  that  or equal  i n envelopes  contact,  monzonite  i s crosscut veins  (Plate  around  where  illite,  found  calcite  Zone  fracture  porphyry)  identified  by c l o s e l y  eventual  disappearance  outwards  from  transition  spaced  and m a f i c  t o s e r i c i t e and s m a l l  and  of abundant  2.9). This  as a c o l o u r change  zone  zone  change  - 24 -  zone  chlorite  (thermal  i s marked  of  such to a  ( F i g . 2.1: of the  minerals amounts of  include  hematite.  and t h e p r o p y l i t i c  the b i o t i t e a l t e r a t i o n  i s seen  of  d e s t r u c t i o n of p l a g i o c l a s e  locally in this  of b i o t i t e  can  contact  2.7). Bleaching  (V):A transitional  by t h e a p p e a r a n c e  the rock  i s reduced  1.3 a n d 2 . 1 : b i o t i t e - c h l o r i t e s u b z o n e ) e x i s t s facies  some  of the o v e r l a p p i n g  of o r t h o c l a s e  and c h l o r i t e )  minerals  alteration  t o 10 f r a c t u r e s  v e i n s . The s o u t h e a s t  of the complete  2.2.1.5 P r o p y l i t i c  potassic  rocks are  s e r i c i t i z a t i o n o f an i n t e n s i t y  rock  hornblende  kaolinite.  (Plate  occurs  and p a r t i a l a l t e r a t i o n  (biotite,  Figs.  of the d e p o s i t  intensity  of p h y l l i c  ( F i g . 2 . 1 : up t o 100 p e r m e t r e ) ,  pervasive  i s the r e s u l t  feldspar  on t h e i n t e n s i t y  ( F i g . 2.1: l e s s  t o 100 p e r m e t r e ) q u a r t z  rocks  2.8). Fracture  by s e r i c i t e a s a r e s u l t  envelopes exhibits  (Plate  the i n t r u s i v e  a r e maximum  alteration  50  controlling  metre) s e r i c i t i z a t i o n only  quartz  be  volcanic rocks  and  (Table  2.1, and  between t h e a n d c a n be  and a d e c r e a s e  and  hydrothermal)  zone.  I n hand  specimen  this  from  a black  or brown  to green  by i n c r e a s i n g a b u n d a n c e s  of  fine  grained  epidote,  disseminated  a_nd  most  abundant  occur  locally  sericitic  but  preserved  as  pronounced (Plate  In  units  Chlorite, orthoclase, related  to  biotite  replaced  stock  fragments  are  replaced  Dahl  masses  carbonate  occurs  (see  epidote  i t is generally  also  found  zones.  iron-rich are  chlorite  r e p l a c e d ' by  by  studies  of  the  THE  Berg  -  stock  ( P l a t e 2.11)  epidote  25  (Plate  none  coarse chlorite.  is  and  in  -  in  the assemblage  thermal  collapse  t o , or  of  (Table where  spatially  2.2:  type  biotite  is  plagioclase  2.12).  are  is  retrograde  TELKWA FORMATION V O L C A N I C  deposit  present,  increases  This  restricted  porphyry  by  groundmass.  chlorite-carbonate-sphalerite veins common i n t h e  zone  and  1967)  d i s c u s s i o n ) . Where  P O T A S S I U M METASOMATISM OF  Previous  replaced  until  are  become  often  Norton,  biotite  the  rocks,  propylitic  i n the  are  envelopes  the  finer  is  s p h a l e r i t e , however,  subzone,  p r o p y 1 i t i z a t i o n caused  system  i s most by  are  and  carbonate  in volcanic  in  by  and  i n abundance  (c_f_.  irregular  retrograde  phenocrysts  2.3  the  and  Alteration  biotite  o r t h o c l a s e - b i o t i t e and  to,  This  of  and  galena  Fragments the  Pyrite,  chlorite  ( P l a t e 2.9).  decreases  epidote  hydrothermal  related  zone;  chlorite  forms  propylitization  3b).  margins  rich  and  this  from  cores  carbonate.  quartz,  outlines in  The  and  with  developed.  distance  the  iron  abundance  the  poorly  with  and  in  albite  i n some v e i n s  ghost  epidote  whereas  i n veins  sulphide  2.10).  flow  chlorite,  ambiguous  about  ROCKS  the  origin  of the b i o t i t i z e d . rocks  mineralized  z o n e .. P a n t e l e y e v  to  this  describe  unit  and metasomatic  Brown,  Thus  could  authors  or a hydrothermal  A distinction situ  loss,  these  rocks  and metasomatism  exchange  of chemical  solution. reacting control  with  as an a l t e r a t i o n  the rock;  on m e t a s o m a t i c  with  (cf.. S u t h e r l a n d  either  a  little  between w a l l  contact-thermal  hornfelsing  chemical  rock  by f l u i d s  therefore fracture alteration  biotite  origin.  involving  i s caused  hornfels'  true hornfels  c h e m i c a l l y by d e f i n i n g  of a rock  process  'biotite  that the secondary  as h a v i n g  components  The l a t t e r  are present  metasomatic  c a n be made  recrystallization  t h e term  that both  noted  n o t be a s c r i b e d d o m i n a n t l y  metamorphic  in  (1981) used  b u t he s u g g e s t e d  ( i so c h e m i c a l ) 1967).  t h a t c h a r a c t e r i z e much o f t h e  as  g a i n or  significant and a  hydrothermal  permeating  intensity  i s an  and important  and c o n s a n g u i n o u s o r e  mineralization.  In  the v o l c a n i c rocks  potassium minerals  bearing  on a v e r a g e  percentage K  2  mineral  limited  areas  intermediate 1.5%  from  i n the rock  than  contents  orthoclase, sericite 1% o f t h e r o c k .  c a n be u s e d  thermally altered  biotite  those- e x p e c t e d  t o t h e m i n e r a l i z e d zone  i s biotite;  make up l e s s  of b i o t i t e  0% t o d i s t i n g u i s h  adjacent  from  clay  Therefore the  metasomatized  with  rock. In  of 10% t o 20% a r e c o m p a t i b l e  v o l c a n i c rock  and  i n conjunction  the isochemical r e c r y s t a l l i z a t i o n  to mafic  t h e main  with  o f an  a K 0 c o n t e n t o f 1.0 t o "2 up t o 1 4 % b i o t i t e ) . I n t h e p o t e n t i a l o r e  ( 1 % K 0 w i l l form 2 zone, p a r t i c u l a r l y where  with  mineralization  -  26 -  i s evident, biotite  contents  r b AI 0 *Fe 0-(K 0 •Na 0*CaO) 2  2CaO  3  2  2  (CaO*MgO*Na 0)  2  Kp+Nap  2  2K 0 2  a  L F i g u r e 2.2 M a j o r e l e m e n t t e r n a r y p l o t s t h a t c o m p a r e t h e b u l k compositions of the r e g i o n a l Telkwa Formation v o l c a n i c r o c k s (field A: f e l s i c m e m b e r s ; f i e l d B: m a f i c t o i n t e r m e d i a t e m e m b e r s ) w i t h a l t e r e d and h o r n f e l s e d r o c k s from t h e m i n e r a l i z e d . z o n e ( f i e l d C ) .  reach  50%  (K  0 values 2 Whole r o c k  potassium. vicinity  of  relatively Richards,  the  5.0%  to  7.5%)  chemistry  of  the  m i n e r a l i z e d zone  fresh, 1976)  illustrated  from  albeit  in Figure  2.2a,  this a  'altered'  compared  distant,  demonstrates  indicating  to  the  a d d i t i o n of  volcanics in chemistry  regional equivalents gain  ternary  i n potassium. plot  of  (Tipper  This  0 - (K 0 + Na 0 + CaO) vs. (CaO + MgO + Na 2 3 2 2 2 r e p r e s e n t a t i v e samples of Berg a l t e r e d v o l c a n i c s ( f i e l d  B)  have  rocks  e q u i v a l e n t s of been  plot  i n two  intermediate representing (C)  plotted.  cluster  Telkwa  Figure  distinct  2.2a  Formation shows  i n the of  Formation  high the  fields,  K 0 2  a  and  is  C)  and  volcanics (fields  that  the  Telkwa  A  and  Formation  K 0 f i e l d (A) c o n t a i n i n g 2 a n d m a f i c v o l c a n i c r o c k s , and a h i g h K 0 f i e l d (B) 2 f e l s i c v o l c a n i c s r o c k s . Berg a l t e r e d v o l c a n i c a n a l y s e s  representative Telkwa  the  of  2 x K 0 v_s A l 0 + 2 2 3 0 ) , where  Fe  regional  the  field.  intermediate  (Panteleyev,  low  L i t h o l o g i c a 1 1 y , however,  they  and' m a f i c  of  1981;  van  der  volcanic rocks Heyden,  1983,  are  the  personal  communication).  Figure  2.2b  i s a ternary  plot  of  2 x CaO  (K  0 + Na 0 + CaO) v s K 0 +Na 0. H e r e T e l k w a 2 2 . 2 2' r o c k s p l o t i n an e l o n g a t e f i e l d t r e n d i n g f r o m B:  felsic  rocks)  volcanics). CaO  field.  Potassium binary  This  of  h i g h ' CaO  altered  values  thus  (field  volcanic rocks  i s consistent with  enrichment  plot  Formation  Berg  to  A:  (field  their  i s demonstrated  Ca0%  v_s_ A l 0 + Fe 0 2 3 2 3 Formation v o l c a n i c  28  -  CaO  values  intermediate C)  plot  original simply  _y_s K 0% w h e r e i n t e r m e d i a t e 2 v o l c a n i c r o c k s p l o t c l o s e t o t h e CaO  -  low  to  (field  and  i n the  mafic high  lithologies. by  Figure  mafic  a x i s and  2.3,  a  Telkwa the  felsic  \  10  ^  Telkwa Fm.  •  Telkwa Fm. Felsic volcanics.  . \  •  Berg  Intermediate and mafic volcanics  altered volcanics.  •  * i  -8  oo o  •  •  /  /  /  \  \ •  •  VI/ 2  /  VI  V  ^ •.  3  \0  % K0 2  F i g u r e 2.3 CaO a l t e r e d Telkwa  vs K O p l o t demonstrating potassium enrichment of the F o r m a t i o n v o l c a n i c r o c k s from the m i n e r a l i z e d zone.  - 29 -  units  plot  volcanic  that the  in  the  for  a metasomatic zones.  metamorphosed ore  zones  intrusion  Ore  and  rather  In  origin  addition,  volcanic are  than  rocks  spatially  to  for  the  the.altered  field are  Berg  mapping  present  related stock  volcanic  to  away  the  (Fig.  has  shown from  quartz  1.2).  Mineralization  Hypogene dominated  have  of  also  1981).  ore  by  bornite,  amounts  mineralization  pyrite,  ore  pyrite  zone  sulphide  contents  hypogene  ore  established  by  chalcopyrite  can  be  This  defined a  to  (Stewart, to  over  rarely  minerals  the  and  scheelite,  reported of  50:1  exceed  ilmenite, 1967;  the  5%  by  visually  chalcopyrite  forms  an  almost  i t s contact.  ratio  continuous  Width  10  -  1973;  Panteleyev,  halo  (Fig.  to  From  The  an  less  ring  the 2.1).  element  economic  hypogene  chalcopyrite of  in  zonation  trace  than  ranging  ore  4:1  of zones  zone  the  which  exceeding  (Fig.  from  Total  viewpoint  contents  surrounding  trace  arsenopyrite  pyrite  is variable,  -  and  is  quantities and  1:1  potential  estimated  Small  from  closely  the  deposit  range  volume.  zone  Berg  galena  rutile  Howard,  et, a l . ( 1 9 8 3 ) .  by  the  tetrahedrite,  Heberlein  outlines  at  molybdenite.  in  corresponds  to  straddling  2.2)  chalcopyrite  pyrite  zone  and  sphalerite,  pyrrhotite,  Ratios  (Table  chalcopyrite  magnetite,  been  potential  1%  0 a x i s . I t f o l l o w s that Berg a l t e r e d 2 i n a f i e l d o f h i g h CaO and h i g h K 0, t h u s • 2  MINERALIZATION  2.4.1  of  K  mineralized  thermally  diorite  the plot  evidence  potential  2.4  to  analyses  providing rocks  near  2.1).  stock  less  and  than  100  m at  the  west  contact  contact  w h e r e -the  altered  volcanic rocks  Molybdenite annular  zone  within  halo  and  the  that  occur  quartz  though  150  m  responsible  for  2.2:  3b).  type  2.4.1.1  locally  zones  Hypogene  generally  economically  concentrations  sulphides the  occurs  deposit.  occurs  exceeds  2%  0.2% by  grade  i n the copper)  at  the  m  in  the  (Panteleyev,  1981).  conform  similar  at  the  to  i n the the  contact.  i s concentrated between  propylitic intrusive  occurs  the  mineralization: whole  important  0.5%  to  and  zone contact.  may  be  within  the  hosted  diorite  i n the  northeastern  the the  volume.  31  -  sulphide core  they  disseminated part  of  mineralization also  of  the  stock  deposit  are  relatively  total  are  sulphides.  in  of  -  vein  although  copper  unfractured  because  than  (Table  Disseminated  1.0%.  disseminated  center  deposit,  in  the  Galena  t e t r a h e d r i t e which values,  a  intrusive  ( F i g . 2.1).  of  northeast  quartz-chlorite-carbonate veins  quartz  relatively  grades  than  of  m  transition  zones  silver  over  less  i n the  Lower  i n the  example, (less  widespread  the  500  disseminated  are  400  deposit,  veins  minor  in late,  sulphides  However  and  high  the  with  i n sub-economic  associated with  ore  diorite  sporadic,  alteration  Sphalerite,  potential  over  c h a l c o p y r i t e zone  conforms  approximately  to  m i n e r a l i z a t i o n i s hosted  throughout  propylitic  sphalerite between  and  ubiquitous  pyrite  biotite  hypogene  occurrences,  Pyrite, the  best  ( F i g . 1.2)  sulphide  (zone  content  I ) . For low  rarely  2.4.1.2 Hypogene potential  of  veins  relationships.  shows  were  vein  that  the  earlier  and  they  and  gypsum, have  close (types  by  3b)  are  alteration  they  are  invariably  encountered  earliest monzonite These  discontinuous,  generally  late  veins  in  and  are  composed  4a),  the  vuggy, milky  32  -  carbonate of  the  bearing  permeability, bearing  contact  alteration  paragenetic  pyrite  molybdenite  further  from  by  Distribution  fracture  veins  although  zones  where  sequence.  are  characteristically  -  temperature  dominated  and  high  2.3)  2a)  biotite,  higher  restricted  plagioclase biotite  of  l a , l b and  carbonate  l a ; Plate  and  of  copper  potassic  Table  molybdenum  envelopes.  of  4a,  mineral  alteration.  orthoclase,  and  and  of  C h l o r i t e and  the  the  (type  porphyry veins  in  3b  3b,  sphalerite, chlorite,  zones  and  stock.  3a,  basis  (types  suggestive  along  rarely  the  (types  and  with  concentrated  are  quartz  are  contact.  several  3a,  envelope  copper  earlier  intrusive  the  generations  the  accompanied  they  The  vein  which  sericite  on  in adjacent  associated  veins  l a , l b , 2a,  the  the  3a  types  identified  of  of  the  megascopic c r o s s - c u t t i n g  indicates that  were to  are  anhydrite  mineralization  fluids  and  f o r most  Later  types  by  be  the  environments.  vein  can  in  mineralization;  and  defined  2.2,  responsible  magnetite  p r i m a r i l y in veins  Individual vein  i n Table  assemblages 2.2  mineralization: Mineralization in  o r e "zone i s f o u n d  generations  defined  vein  porphyry  to  phases  irregular,  quartz  with  the  common  of  TABLE Vein  2.2  Vein  Type  and  a l t e r a t i o n envelope  Mineralogy  la 1 b ( 1) 2a(l) 2a(2) 2a(3) 3a(l) 3a(2) 3b(l) 3b(2) 3b(3) 3b(4) 4a  mineralogy-  Envelope  Dominant  Qz-Ms -Or - B i Q z - B i -Ms (Cl-Ep) (Ms.) none none Qz-Ms (Ms) Ms none (CI) Ms none  " Qz Qz -Py -Cp-Mo Qz -Mo Ah -Mo Mo Qz -Py -Mg-Cb-- C I Qz -Py ( C p ) Qz -CI- - C b - S l ( M s - G y ) Qz -CI- - C b - S l ( M s - P y ) Py. - C I - C b - S l (Ms ) Qz -Cb Gy  Origin  magmatic ma gma t i c magmatic magmatic magmatic meteoric me t e o r i c me t e o r i c me t e o r i c meteoric meteoric meteoric  V e i n t y p e s d e f i n e d i n t e x t , a r e i n o r d e r o f r e l a t i v e age (type 1 a r e the o l d e s t ) . Numbers i n p a r e n t h e s e s d e f i n e s u b d i v i s i o n s of general vein types. M i n e r a l s , l i s t e d i n o r d e r o f a b u n d a n c e on a v o l u m e % b a s i s , are coded: An=anhydrite, Cb=carbonate, C l = c h l o r i t e , Cp = c h a l c o p y r i t e , G.y = g y p s u m , Mg=ma gne t i t e , Mo = m o l y b d e n i t e , Ms=muscovite ( s e r i c i t i c ) , Or=orthoclase, Py=pyrite, Qz=quartz, Sl=sphalerite; brackets i n d i c a t e possible presence.  anhydrite  cavity  but  when  and  significant  veins.  present  They  are  surrounding a  zone  of  the  these type  consist in  terms  molybdenum  2a  More  veins. milky  anhydrite  or  occur  throughout  of  secondary  of  sulphide  volcanic  s t r a d d l i n g the  veins.  A l t e r a t i o n envelopes  of  rocks,  are  quartz  dominated  veins,  or  the  the  by  as  veins.  zone.  -  33  to  Much of  zones of  are  and  Highest but  as  are  be  part  found  stringers  of  in  with  disseminations  can  lb  the  and  associated  A l t e r a t i o n envelopes  -  and  copper  densities  they  type  concentrated  molybdenum  streaks  the  stock  be  absent  widespread  are  the  molybdenite  i n t r u s i v e contact,  mineralized  porphyry  appear  quantities  quartz-anhydrite  near  but  p o t e n t i a l ore  significant  These  the  generally  More  mineralization  i n t r u s i v e contact. the  are  orthoclase.  d i s t r i b u t e d throughout  altered  ribboned,  type  fillings.  this  in  in in vein  found are  generally  absent  but.where  present  are  less  1 mm  than  wide  zones  of  and  2 in  sericitization.  Type  3a  veins  chalcopyrite envelopes Where  and  result  envelopes  from  of  the  type  3a  the  with  the  veins  the  quartz of  of  and  and  alteration quartz.  completely  envelopes. intrusive  monzonite  pervasive  type  decreases  that  3a  deeper  are  of  pyrite.  Type  3a  contact  stock.  at  the  These  phyllic  vein  destroy  veins  d i s s e m i n a t i o n s of wide  at  zones  overlapping  sericite  m i n e r a l o g i e s . The  and  developed of  by  1  In a d d i t i o n ,  overlap  stringers  edge  closely  absent.  dominated  within  types  alteration  envelopes.  i n the  explored  part  of  deposit.  Type  3b  veins  present  outwards and  with  northern  from  t e x t u r e s and  intensely  correspond  Abundance  are  these  quartz  i s most  southern  that  i n t e n s e and  also i s disseminated  veining  areas  different  molybdenite  structures,  to white  Pyrite  the  more  developed  pre-existing grey  very  i s r a r e and  are  best  are  throughout  from  pyrite  the  are  present  these  (Plate  the  where mafic  v e i n s may  deposit  intrusive  wall  where  sericitic replaces  by  the  rock veins  they  be  these  '2.9).  wall  similar  chlorite  rocks  rich  to  type  type  -  34  3a  -  of  zone.  sphalerite  is  Quartz is a  carbonate  in biotite,  vein,  veins  controlled  and  rocks.  but  These  abundant  propylitic  mineralogy  intrusive  in this  carbonate.  become more  i n the  composition; cut  and  veins; black  Vein  crosscut  minerals  but  contact  u b i q u i t o u s to  common a c c e s s o r y partially  c o n t a i n much c h l o r i t e  but  Chlorite indicating  reflect  are  effects  are  commonly that of  wall  P l a t e 2.9 P r o p y l i t i c a l t e r a t i o n ( z o n e V) o f b i o t i t e h o r n f e l s . This dark green rock i s s o f t e r and l e s s m a s s i v e t h a n o r i g i n a l b i o t i t e h o r n f e l s a l t e r a t i o n ; o r i g i n a l h o r n f e l s i c t e x t u r e s are preserved, N o t e the o u t l i n e s of volcanic fragments (dotted o u t l i n e s ) . The v e i n a t the top of the s a m p l e i s a l a t e t y p e 3b c a r b o n a t e chlorite-sphalerite vein.  P l a t e 2.10 Formation visible. L r i m m e d by trachytic  G r e e n p r o p y l i t i c a l t e r a t i o n ( z o n e V) o f T e l k w a volcanic f r a g m e n t a l r o c k . O r i g i n a l t e x t u r e s are clearly i t h i c f r a g m e n t s a r e r e p l a c e d by c o a r s e e p i d o t e and f i n e g r a i n e d e p i d o t e and c h l o r i t e . G r o u n d m a s s has a texture. -  35  -  P l a t e 2.11 R e t r o g r a d e p r o p y 1 i t i z a t i o n of q u a r t z m o n z o n i t e p o r p h y r y ( c r o s s e d n i c o l s ; s c a l e b a r i s 1 mm). Igneous b i o t i t e ( B i ) , p a r t i a l l y e n c l o s e d i n q u a r t z ( Q z ) , h a s b e e n p s e u d o m o r p h e d by iron r i c h c h l o r i t e ( C I ) . Note a l s o the i n t e n s e c l o u d i n g of p l a g i o c l a s e p h e n o c r y s t s ( P f ) by f i n e s e r i c i t e a t b o t t o m o f v i e w .  P l a t e 2.12 Retrograde p r o p y l i t i z a t i o n of p l a g i o c l a s e biotite p o r p h y r y ( p l a n e p o l a r i z e d l i g h t ; s c a l e b a r i s 1 mm). Sericitized p l a g i o c l a s e ( P f ) i s r e p l a c e d by i r o n r i c h e p i d o t e ( E p ) . A b i o t i t e ( B i ) p h e n o c r y s t a t the b o t t o m l e f t of t h e v i e w has been replaced by i r o n r i c h chlorite. -  36  -  rock  composition.  The  youngest  vein  fractures.  These  are  greater  rarely  gypsum  veins  up  These  probably  veins  with  This  mm  i n width  formed  by  r e a c t i o n of  gypsum-filled  sub-horizontal attitudes  in width.  30  by  are  Coarser also  grained  fibrous  common i n t h e  hypogene  and  anhydrite  intrusion. bearing  waters.  of  undoubtedly  vein  vary  types  along  vein  types  l b and  of  i s g e n e r a l i z e d because  their  length.  veins  are  vein  In a d d i t i o n  recognized  by  2a.  DISCUSSION  A model altered  of  and  Events  brittle  intrusion  the  sequence  of  m i n e r a l i z e d zones  compared  Ground a  2 mm  multiple generations  crosscutting  2.5.1  than  to  i s represented  g e n e r a l l y have  classification  complicated  and  veins  ground  compositions  2.5  generation  to  recent  Prior  to  (Figs.  at  Berg  the  e v o l u t i o n of  deposit  i s proposed deposits.  similar  porphyry  Emplacement  o f Berg  Intrusion  the  h o r n f e l s zone 1.2  the  during  s t u d i e s of  preparation' for biotite  events  and  1.3).  -  deposit around  began the  I n t r u s i o n of  37  -  with  quartz the  the  below'  formation  diorite  Berg  the  quartz  of  monzonite fracture bodies. zone  into  the  zones From  h o r n f e l s and  i n the  field  by  hornfels that  observations  associated with  overprinting  quartz  the  hydrothermal  became  the  quartz  diorite loci  presence  monzonite  processes  developed  of  stock  would  intense  for potential a minor, cannot  ore  hornfels  be  have masked  ruled such  out;  a  zone.  Potassium-argon diorite (circa  and 50  and  the  quartz  Ma).  Panteleyev than  the  ( 1976,  distribution  of  pointed  the  out,  hydrothermally of  the  represent  of  because  1983,  a  (circa  phases  at  82  sample  by  K-Ar  described  1.2  2.1  basis  that  north  by  date  stock.  The  south or  and  with  Lake  ( 1 9 8 1 ) and Berg  intersects  38  the  -  of  was  reset  to  might  suggested  closely  1981).  stock  at  the either by  (Panteleyev, to g r a n o d i o r i t e  The  illustrated  deposits  intrusive in  monzonite,  fragments,  (1981)  altered  property  quartz  quartz spatial  copper-molybdenum  1974,  monzonite  -  the  alteration  Panteleyev  as  by  older  the  diorite  intrusion  correspond  Ox  the  quartz  probably  of  the  and  ( 1 9 8 1 ) was  quartz  comagmatic  of  intrusion  As  and  diorite.is  diorite,  this  Panteleyev  probably  the  Carter  dating: Carter,  i t contains and  quartz  quartz  author  superimposition  by  the  the  quartz  porphyry,  the  by  dated  to  i s oogenetic  the  f o r the  indistinguishable  ( F i g . 1.2).  older  found  are  hornfels  Huckelberry  breccia and  into  communication),  the  Ma  the  therefore  slightly  personal  porphyry  dikes  quartz, monzonite  monzonitic  the  stock  of  1981)  observations that  biotite  and  field  stock  1981 ) s u g g e s t  m i n e r a l i z a t i o n zones porphyry  ( C a r t e r , 1974,  monzonite  However,  porphyry  monzonite  age  dates  Figures on  the  dips steeply  depth.  This  to  breccia  2.5.2  also  crosscuts  Magmatic  Magmatic quartz early is  hydrothermal  s i m i l a r to  1975)  development  at  Ajo  with  of  the  that  accompanied  magmatic  to  away  Burnham,  1979;  1972,  deposition  the  heat  and  to  release  the  Yandara  of  the  of  pressure  and  Nash,  sealing  the  center  magmatic  and  the  of  the  rocks  explains  were  brittle  fashion.  Specifically,  suggest  that  rocks  were  stock  stock less  deformed  behaving  -  39  -  of  1974;  reflect the  where  locally  that as  the  fluids  Beane,  1982;  Roedder, by  (from  mineral  hydrostatic  veining  this  fail  la quartz in a  melt  of  events  process.  r e l a t i v e lack  to  the  and  evolution  conditions  likely  in  above  fractures  Multiple  type  and  hydrous  1979;  changes  failure.  the  also  rocks  (c_f. B a r n e s ,  periodic  rock  magma, 2)  Rita  (cf .  development  crystallization  Moore  Santa  early  processes  wall  Alteration  (Grant  crystallizing  fracture of  1982),  the  that  unit.  occurring  following  i n t e r n a l pressure  towards  the  and  source  margin  this  1946)  surrounding  1970;  3)  to  Aiken,  the  on  suggesting  and  during  resulting in  Periodic  nearly  the  caused  close  stock,  related  boundary  fluids  i s centered  (West  extensive  with  1979),  observed  veining  by  Helgeson,  lithostatic)  the  metasomatism  by  solidus  from  that  of  Berg  d i f f e r e n t i a t i o n of'a  reacted  migrated  to  (Gilluly,  hydrothermal  extensively  1971,  1)  the  Sierrita  deposit  1979):  peripheral  phase  potassium  Burnham, was  processes  p r o c e s s e s . were  that  1968),  diorite.  a l t e r a t i o n at  porphyry  hydrothermal  Neilsen,  quartz  hydrothermal  monzonite  (Neilsen,  the  of  were  in  a  veins  plastic  fashion.  Chemical monzonite addition  reactions  stoc-k m a i n l y of K  orthoclase, to  produce  As from  +  those  above,  of igneous colour.  biotite  suggests ++ a n d Fe  are  +  potassic  i o n exchanges.  ++  o f K , Mg  hydrothermal  origin  , OH  close  orange-brown  biotites  on t h e b a s i s  The c o l o u r  i n primary  Hydrothermal  change,  biotite  observed  that  t h e c o m p o s i t i o n has been  from  the igneous  biotite  to secondary  biotites  magnetite,  to  amphibole  c a n be  distinguished  i n the country  t o g r e e n i s h brown w i t h  the a l t e r e d  alteration  volcanic  rock  t o show a s i m i l a r  ratios  outwards  made a t - B i n g h a m (Jacobs  from  and P a r r y ,  trend  from  high  and Czamanske, 1976) where  the c e n t e r of the system  altered.  ilmenite  from  Liberation likely and  i n Mg  rutile  40 -  from t h e to t o t a l  Fe  and N o r t o n to t o t a l  o b s e r v a t i o n s have  1 9 7 3 ) and a t E l y and  hydrothermal  (MgO) a n d d e p l e t e d i n T i O w i t h 2  pale  Chlorite^ compositions  t o l o w Mg  are s i g n i f i c a n t l y  -  from  distance  r e p o r t e d by D a h l  the stock. Similar  (Moore  section,  i n secondary  change  increasing  to c h l o r i t e .  r o c k s were  (1967)  i n thin  biotite.  o r by p a r t i a l  component  t o form  a r e t h e most  ratio,  to  are the  and F  to orange-brown  T h i s c a n be e x p l a i n e d by t h e a d e c r e a s e  Rita  Examples  o f t e x t u r e and  stock.  in  of the quartz  a n d Ca i n plagioclase + ++ -  as o x i d e m i n e r a l s i n c l u d i n g  common  alteration  biotite.  brown  changes  o f Na  and t h e a d d i t i o n  reddish  TiO 2  involved  and l o s s  mentioned  pleochroic  of  producing  biotites  richer  Fe  been Santa nearer  i n phlogopite  respect to primary  biotites .  Early 2b)  were  are  the  vein  contemporaneous earliest  plastic  Rita  of  similar (Jacobs  Type the  was  2a  and  rock  C have form  and  1976); of  adjacent  country  rock.  In  sulphide  have  c o o l i n g due  wall  rock  be  alteration.  noted  above.  obtained  and  the  vein  anhydrite  + Fe  Variable  of  the  quartz  pressure  r e l e a s e , Eh-pH c h a n g e s  g e n e r a l i z e d by  2H  S +  2 . 2  of  suggest  important  Furthermore,  Santa gave.  1971). and  deposition Sulphide  that  include:  due  interaction  to  with  minerals).  reaction 1 (cf .  veins  stock  precipitation.  bearing  magmatic  wall the  Sulphide  Beane,  1982):  + +  amounts  deposit  implying  assemblage) at  s e v e r a l causes  iron  veins  veins  from  of  and  similar  type  chemical  la  Nearly  from  periphery  ++  + Cu  Type  i n shape  alteration  this  reactions, direct  can  l a , l b , 2a  resulted  ( i . e . replacement  precipitation  an  to  types  Bingham e a r l i e s t q u a r t z o o 640 C t o 725 C (Roedder,  near  could  2.2:  at  occur  by  as  been  b veins  alteration  played  pervasive  wall o  800  Parry,  (Table  generally irregular  temperatures  rock  the  to  Berg  and  deposition  of  up  accompanied  sudden  are  mineralogy,  homogenization  in  and  at  with  c o n d i t i o n s i n the  temperatures (i.e.  generations  = CuFeS  disseminated that  role  replacement  1/40  3H  +  d e p o s i t i o n of  41  -  2  interaction  0  must  sulphides.  iron-bearing minerals  -  1/2H  1_  mineralization in a l l parts  wallrock/fluid  i n the of  2  +  by  copper  have  sulphides  a n d p y r i t e i s common  a n d may  be g e n e r a l i z e d  by  reactions  2 t o 4:  Fe  0  + 3Cu  +  + 6H S + 1/40 = 3CuFeS + 3H 2 2 2  3 4  +  2  + 9/2H 0 2  or  KFe(AlSi)  0  (OH)  3 10 KA1  + 4Cu  +  + Fe 0 + 6H S + 3/40 = 3 4 2 2  2  • +  Si 0 + 4CuFeS + 8H 0 + 0 + H 3 3 8 2 2 2  or  + 2KFe  3  AISi  +  0 (OH) + Cu 3 10 2  + 2H S + 0 + 12H 2 2 -  Fe  A l S i 0 (OH) 5 2 3 6 8  + CuFeS  =  +  + 2K  + 3 S i O ' + 6H 0 2 2  2  4  + Note  that  reactions  1, 2 a n d 3 l i b e r a t e  •with  the e f f e c t of d e c r e a s i n g  H  +  ions  into  the s o l u t i o n  +  the K  to H  ratio,  at least  locally  + adjacent  to veins.  chemistry of  i s stable  orthoclase.  sericite  envelopes  orthoclase The  This  If sufficient with.respect probably around  H  i s l i b e r a t e d the s o l u t i o n  to s e r i c i t e ,  explains  many  type  causing  the presence  l b and 2 v e i n s  of  destruction thin  i n the  zone.  a s s o c i a t i o n of anhydrite  with  - 42 -  sulphides  i n type  l b and 2  signifies  a third  documented  by  hydrothermal  possible  Holland fluid  precipitation  and  Malinin o 600 C to  from  mechanism  that  has  been  ( 1 9 7 9 ) . C o o l i n g of a magmatic o 400 C c a u s e s o x i d a t i o n of SO 2  to  H  SO  (equation  2  5):  4  4H  0 +  4S0  2  Increased  = H 2  a c t i v i t y of the 4 liberated during orthoclase  (Ca will  SO  cause  anhydrite  + H 2  Removal  of  SO  4  of  (equation  =  CaSO  4  +  presence calcic  of  CaCl ' 2 plagioclase)  6):  2HC1  4  from  4 activity  SO 2  replacement  SO 2  3H  s o l u t i o n i n the  precipitation  CaCl  S + 2  thus  solution concomitantly r a i s e s the H S • 2 p r o m o t i n g s u l p h i d e p r e c i p i t a t i o n and sulfidization  reactions.  Molybdenite in  a narrow  stock.  This  generally  annular zone  zone  is restricted adjacent  i s o u t l i n e d most  to  to  the  clearly  type  outer by  2 veins margin  grade  that  of  occur  the  distribution  ( P a n t e l e y e v , 1 9 8 1 ) a n d by s t a t i s t i c a l m e t h o d s ( F i g . 3.4) 2 • F l u o r i n e e n r i c h m e n t o f t h e s t o c k , as d e m o n s t r a t e d i n H e b e r l e i n  of  MoS  a l . (1984),  i n d i c a t e s that  the  hydrothermal  and  p o s s i b l y as  molybdate of  fluid  fluoride  (Westra  i s extremely  and  was  Keith,  43  -  1981).  likely  (e.g.  ( I s u k - and  temperature  -  most  complexes  chloride, disilicate  complexes  molybdenum  as  molybdenum  et  transported in o MoF a n d MoO F ) 4 3  Carmen, Because  dependent  1981) the  (Smith  and  solubility  e t ..a 1 . ,  1980),  cooling  of outward  fluids  would.result  migrating,  i n rapid  deposition  zone.  Bloom  based  on f l u i d - m i n e r a l e q u i l i b r i a .  fluorine  orthoclase state  (1983) i n f e r r e d other  bearing  phases  under  isothermal  o f t h e molybdenum  demonstrate  with  their  of m o l y b d e n i t e  controls  wall  These rock  involved  r e l a t i o n s h i p , such  confined  deposition  particularly  Depending  on t h e o x i d a t i o n  c a n be w r i t t e n t o  as (Bloom,  0 + MoF 3 8 4  i n a  r e a c t i o n s of  minerals,  conditions.  hydrothermal  f o r molybdenum  ioncertain reactions  3KAlSi  KA1  molybdenum-bearing  1983):  + 2H S =  2  o Si 0 F +6S10 + MoS + 2H 0 + 2KF 3 3 10 2 2 2 2  _7  or  3KA1S1 0 + 4MoO F 3 8 3 KA1  Note  that  both  minerals  in  +  =  o Si 0 F + 2KF + 6 S i 0 +4MoS +10H +70 3 3 10 2 2 2 2 2  both  quartz occur  Precipitation from  + 8H S + 4H 2  i n type  o f Na  their  (equation  of d i s i l i c a t e + + or K  (fluoromuscovite)  2 veins'or  of m o l y b d e n i t e  destabilization  the presence  and m u s c o v i t e  complexes  i f reduced  solution :  -44.-  are formed;  envelopes  10) a l s o  8  (Table 2.2).  can r e s u l t  by HC1 ( e q u a t i o n  sulphur  9)  i s available in.  2Na  +  Mo  No  temperature  however  fluid  produced  ++++  + Mo S i 0 + 2HC1 2 25  ++++  data  inclusion  a range  +  are  = 2Mo  +  2SiO  .+ 2 N a C l  + H 0 2  2 2H S = MoS + 4H 2 2  available  studies  from  o ftemperatures  +  10  for vein similar  9  t y p e s ' a.t  Berg,  d e p o s i t s have  f o r q u a r t z i n the  molybdenite  b e a r i n g v e i n s . For example, h o m o g e n i z a t i o n t e m p e r a t u r e s from 350 o C ( Q z - M o S - O r - A h v e i n s f r o m M i n e r a l P a r k , A r i z o n a : W i l k i n s o n e_t 2 o a l . , 1 9 8 2 ) t o 650 C (Qz-MoS v e i n a t B i n g h a m : M o o r e and N a s h , . 2 1974). Veins e x h i b i t i n g p o t a s s i c a l t e r a t i o n envelopes ( i . e . orthoclase,  biotite  at  E l Salvador  at  Sierrita  related  high  Berg  and  and  Gustafson,  Beane,  1982)  imply  that  fluid  fluids  hydrothermal  Hydrothermal  alteration  o f the  magmatic  different  bulk  inclusions NaCl  early  vein  temperatures.  i n these  veins  gave  e q u i v a l e n t range a t for this  type  of veining  origin.  Rocks  a sequence  that  t ohigh  responsible  of. Country  escaping  implying  37 t o 41 w t . %  Alteration  reflects  o t e m p e r a t u r e s o f 525 C o o 1 9 7 6 ) a n d 300 C t o 370 C  yielded  o c c u r r e d at moderate  ( i . e . i n the  o f magmatic  2.5.3  of  ( P r e e c e and  q u a r t z ) have  d e t e r m i n a t i o n s from  values  Sierrita) are  (Sheppard  alteration  Salinity  and  hornfels  of physical  hydrothermal  fluids  c h e m i s t r y and  and  45 -  biotite  c h e m i c a l changes  as they  move a w a y  -  t o the  from  permeate the  heat  zone a t in  wall  the rocks  source.  Models  of  (Norton, is  fluid  upwards  a  zone  This the  and  with  of  1970) from  inward  mixing  at  zone  to  country  the  rocks  chemistry  of  relatively minerals ++ Fe and  the  rich  ( i n s t e a d of  biotite  Fe  were  porphyry  country in  were  mechanisms  probably  the  available from  rocks.  abundant  the to  those  The  reactions  migration  increase  i n the  of  most  Fe  of  bulk  which  were  the  same  time  and at  Cook,  the  veins  the  1982).  biotite  suggest  source  stock  and  biotite.  zone  orthoclase-biotite  likely  i n the  -  at  the  bearing  modal  - 46  of  by  with  ferro-magnesian  and  part  Close  the  i s developed  (Koski  inner  pyrite  in solution.  Outward  pronounced  for  mineral  interacted  orthoclase  zone  in Arizona  similar  biotitization  Pre-existing  A similar  from  i s present.  rocks  TiO  H o w e v e r , more  was  volcanic  i n the  and  reflects  M g - r i c h - b i o t i t e and as  contact.  dominated  by  Deposition  was  assemblage  replaced  liberated  occurs  transition  fluids  were  deposit  Fe  zone  and  2  waters  that  intrusive  assemblages  orthoclase)  Ca.  fluids  Berg.  Mg  Christmas  zone.  at  systems  of  and  the  i n Fe,  zones.  Berg  the by  zone  hornfelsed  orthoclase-biotite  at  from  hydrothermal an  movement  source  the. b i o t i t e  produced  copper  heated 'meteoric  mineral  magmatic  development  initial  magmatic  propylitic  through  and  i n porphyry  i s represented  in alteration  intrusion  Biotite  the  outwards  that  some d i s t a n c e  biotite  the  imply  migrating,  probably  gradation  transport  their  zone  compositions  the  away  ore  mixing  A  to  and  1982;- R o s e ,  interaction in  flow  and  sulphur  abundance  of  that  for  reduced  surrounding is  reflected  pyrite  with  distance  from  in.solution  to  chalcopyrite and of  the the  fluids  the  s t o c k . The  be  of  magmatic results  traveled  d e p o s i t e d . i n v e i n s and  and/or  onset  iron  pyrite.  The  outward  chloritization hydrothermal  i n the  sudden  the  disappearance  with  dumping  from  of  signify  of a n h y d r i t e  increased mixing  groundwaters. dissolved  Mixing  In a d d i t i o n  incorporated  into  changes  -anhydrite  and  hydrothermal propylitic of  meteoric  changes  in fluid the  are  and  dominated  include  albite  i n the  caused  by  subzones  mixed  the or  meteoric  anhydrite.  As  anhydrite i s deposited only temperatures,  delineate  the  outer  Anhydrite  was  used  to  outline  The complete of  limit  of  extent  way  potassic  i n t e r v a l , between  the  disappearance  magmatic  of  biotite  hydrothermal w i t h the  potential  ore  and  outlined  by  alteration  chloritization  meteoric  fluid  zones  maximum  bodies, thus  of  -  can  biotite  magmatic and Onset by  be  the of fluids  used  to  alteration. by  Corn  (1975)  zone.  a n h y d r i t e and  the  r e p r e s e n t s the  mixing.  suggesting that  - 47  The  hydrothermal  Mountain  of  Berg  disappearance  from  a t Red  at  origin.  hydrothermal  the  absence  the  are  zone.  i s indicated  i t s disappearance  magmatic  in a similar  and  of  coincident and  the  biotite,  which  subzone  dominated  processes  chlorite  magmatic  mixing.  of" d o m i n a n t l y  of  near  zone  biotite-chlorite  hydrothermal after  are  Na  propylitic  chemistry  from  + and  biotite  appearance  at  Ca  i n the  whereas of  these  outwards  biotite  origin,  zone  iron  carbonate  Mineralogical reflect  to  of  components  ++ solution.  intrusion  d i s s e m i n a t i o n s as  reactions  fluids  away  It is  fracture mixing  zone  also  intensity was  a  major  control  i n the l o c a l i z a t i o n  Propylitic (Figs.  1.3 a n d 2 . 1 ) was  chemical there  alteration  changes  similar Ford,  formed  by m e t e o r i c  characteristics  dominated  propylitization  increase i n total  i n the overlapping  pyrite  (cf_. E l T e n i e n t e :  fluids.  a r e minor.  iron  h a l o . Many  zone Bulk  However  due t o a b u n d a n t porphyry  Camus,  deposits  1975 ;  have  Panguna:  1976).  2.5.4 T h e r m a l  Cooling migration  Collapse  of the Berg  the effect  and  meteoric  alteration. undergoing chlorite.to  of s h i f t i n g dominated  This  monzonite  form  restricted  preserved.  Lateral  between over  to, first,  green  rocks  fracture  are r e l a t i v e l y  areas  (Table  encroaching  meteoric  encroaching  fluids  are only  2.2) t h a t waters.  with  magmatic  probably  and then  At Berg  intensity  low K  propylitized  - 48 -  to H  Fe-rich  chloritization  in biotitized biotite i s  adjacent  as c h a n n e l w a y s  M i n e r a l o g i c a l changes  relatively  to  zone  retrograde  of i n t e n s e  acted  dominated-  biotite  unfractured earlier  locally  collapse  of the b i o t i t e  biotite,  assemblage.  o f maximum  thermal  earlier  i n p e r i p h e r a l areas  i s c h a r a c t e r i z e d by z o n e s  These  3b v e i n s  inwards  a propylitic  to areas  Where  l e d to the inward  fluids.  the b a r r i e r  fluids  resulted  alteration  propylitization  rocks.  quartz  of p e r i p h e r a l m e t e o r i c  had  type  mineralization.  o c c u r r i n g o u t s i d e of the m i x i n g  accompanying  i s a pronounced  pyrite  of  suggest  ratios  to f o r the  that the.  reacted at  relatively  low  Temperature  temperature  e s t i m a t e s f o r the  a l . (1971) suggest o o 160 C t o 220 C.  Inward at  the  zone  veins,  deposit.  porphyry  collapse  quartz  monzonite  pyrite  (Plate  of  magmatic  to  descend  stock  and  ground and  their  to  with  and  the  occurs  iron  former and  high  into  r o c k s were  alteration collapse.  in peripheral  had  been, a l t e r e d  had  left  rich,  and  previously  potassium  and  the by  preceded of  the  the  s t o c k and  the  assemblage  of  the  that  late  similar  phyllic in  origin;  rocks are c a l c i u m , zones  magmatic  hydrothermal  fluids  -  49  -  of  quartz  in fractured  rocks.  to  development  This  rich  heated  due  latter  aluminum  this  development.  on  implies  the  potassium  sericitized  Here  decline  allowed  s t o c k where  where  to  development  intensity  are  a  and  groundwaters  margins  i n envelopes  areas  3b  of  the  2.8).  Type  allowed  as  stages  quartz, sericite  only weakly  (Plate  of  et  biotite  alteration  fractured  retrograde.propylitization  magnesium  Mg.  of  fracture  deeply  the  plagioclase)  which  rocks favored phyllic  thermal  alteration  cooling  output  of  presence  assemblage  Intensely  corn-position  and  o c c u r r e d i n two  Retrograde  from  with  sericite  documents  the  composition controlled  wall  more m a f i c  by  epidotized  fluid  percolate  rich  fluids  propylitization  system.  system.  Areas  hornfels  chlorite veins  the  zone.  aluminum  and  resulted  hydrothermal into  meteoric  to a p h y l l i c  2.7)  waters  Biotite  the  Fe  a s s e m b l a g e s by S h e p p a r d o 400 C a n d p o s s i b l y as l o w  below  ( a s shown  biotite  i n Ca,  propylitic  Retrograde  of  wallrock  alteration  of  stock  chloritized  downward  rocks high  temperatures  encroachment  Berg  and  with  that that  Low occur that  copper  where pyrite  grades  rocks  have  observations  phyllic  alteration  considerable that  fluids  high  acidity,  replace  been  has r e p l a c e d  Similar  actually  and i n c r e a s e d  pyrite  phyllically  to c h a l c o p y r i t e  altered; textures  p r e - e x i s t i n g oxide  from  many  of the type  other  suggest  and s u l p h i d e  deposits  suggest  ratios  minerals.  that  late  seen  at Berg  i s n o t uncommon a n d  m o d i f i c a t i o n of grades  occurs.  Brimhall  responsible  for phyllic  alteration  low o x i d a t i o n and h i g h  leach  base  original  (1980)  that  suggests  ( c h a r a c t e r i z e d by  sulphidation potentials)  metals  from  pre-existing mineralized  sulphides  with  pyrite,  and s i l i c a t e  zones and  assemblages  with  sericite .  2.6  CONCLUSIONS  Re-evaluation characteristics led  of the Berg  to the f o l l o w i n g 1)  zone  of h o r n f e l s diorite  medium  promoting  cooling 2)  that  monzonite  had p r e v i o u s l y  deposit  has  This  stock  formed  hornfels  was e m p l a c e d around  zone  during  acted  an  into  a  older  as a  brittle  t h e emplacement and  stock.  developed  f o r magmatic  potassium  copper-molybdenum  f r a c t u r e development  of the Berg  channelways  porphyry  quartz  intrusion.  Fractures  and m i n e r a l i z a t i o n  conclusions:  The 50 Ma B e r g  quartz  for  of the a l t e r a t i o n  around  the Berg  hydrothermal  metasomatism  fluids  of the quartz  -50  -  stock  acted  that  monzonite  as  were  responsible  and  surrounding  hornfelsed  volcanic  rocks.  3) I n i t i a l * o r e m i n e r a l replacement minerals) with  reactions  ions  accompanying  deposition  meteoric  pressure  mechanism  occurred  propylitic  of i r o n  and r e d u c e d  sudden  precipitation  and  (of sulphides  o r by r e a c t i o n  copper  that  occurred  disappearance  of anhydrite  propylitization)  the is  release  likely  was  temperatures  Cooling  an  cool,  towards  of m i x i n g  and t h e o n s e t  important ore  of base  less the  mineral phyllic  acid stock.  (outlined  of  simple  biotitization)  ( i n f e r r e d from  with  inwards  by  igneous  the i n t r u s i o n . Later  i n a zone  by t h e  retrograde metal  chloride  and  complexes. orebodies  i n t e n s i t y that  there  stock)  ( l i b e r a t e d during  by d i s a s s o c i a t i o n  4) P o t e n t i a l  Where  bearing  in solution.  encroached  Precipitation  fracture  for iron  occurred  sulphur  within  at lower  probably  a s s e m b l a g e s ) by m i x i n g  waters  bisulphide  deposition  was  no  are l o c a l i z e d within  coincide  pre-existing  a l t e r a t i o n zones  with  altered  hornfels  are telescoped  zones  biotite  o f maximum hornfels.  ( i . e . on t h e w e s t  side  of  and o r e m i n e r a l i z a t i o n  weak.  Applications exploration  of t h i s  around  50 Ma  formed  by e a r l i e r  indicate  to property  and  regional  include:  1) E x p l o r a t i o n  2) T h i n  study  on a r e g i o n a l  monzonite  dioritic  section  favorable  stocks  which  should  have  and q u a r t z  and hand potassic  scale  specimen  intruded  f o r ore zones hornfelsed  dioritic  intrusions.  analysis  c a n be u s e d  a l t e r a t i o n of such  - 51 -  look  hornfels.  to This  zones  alteration ratios  to  can  also  compare  be  demonstrated  using  potentially altered  simple  rocks  with  major  element  fresh  regional  equivalents. 3) vein  Detailed  density  occurrence 4) located  surface  and  over  should  concentrate  d i s t r i b u t i o n , a l t e r a t i o n type  (including  Diamond  mapping  pyrite  drill-holes  zones  of  to  intense  to  chalcopyrite  test  potential  f r a c t u r i n g and  - 52  -  and  on  fracture  and  sulphide,  ratios). ore  zones  potassic  should  be  alteration.  3 M O D I F I C A T I O N S OF  CHAPTER  AND  3.1  GEOCHEMICAL  SUPERGENE  PATTERNS  BY L E A C H I N G  ENRICHMENT  INTRODUCTION  Geochemical has  relied  these  exploration  elements  (Coope,  i n both  mineralization Burnham, trace  element  1973).  ( L o w e l l and G u i l b e r t ,  distributions  processes  by t h e l a c k  dispersion  f o r m e d by  there  of the genesis 1 9 7 0 ; Rose  i n porphyry  systems  1976).  haloes  geochemical  reports firstly  and B e r t , 1979 data f o r  ( e . g .Olade and  Application  of t h e Berg  patterns. This  on t h e g e o c h e m i c a l  hypogene  zone  porphyry  secondly  on t h e m o d i f i c a t i o n  copper  of these  has been an  of porphyry  of these  o f i n f o r m a t i o n on t h e i n f l u e n c e  on t h e p r i m a r y  therefore,  deposits  1982)and i n 1 i t h o g e o c h e m i c a l  1975, 1976,and C h a f f e e  limited  copper-molybdenum  R e c e n t l y , however,  our understanding  1979, T i t l e y ,  Fletcher,  f o r porphyry  on t h e d e t e c t i o n o f s e c o n d a r y  improvement  is  PRIMARY  data  of supergene  chapter,  patterns i n the  molybdenum  d e p o s i t , and  p a t t e r n s by s u p e r g e n e  processes .  3.2 G E O C H E M I C A L  3.2.1  ANALYSIS  Sampling  Outcrops  were' s a m p l e d  holes  on a n o r t h - s o u t h  using  t h e GE0L0G  system  and core  section  collected  from  13 d i a m o n d  of the d e p o s i t . D r i l l  ( B l a n c h e t and Godwin,  - 53 -  core  1972 ; Godwin  drill  was l o g g e d e_t. a l . ,  QFP QMP QPP 1771 P B Q P 1 1 1  „7nr t A i  Breccia  21  Quartz Diorite  o  Hornfels J  t t t' 'tVtVt V t•V - * t.t.t tt t  x> .X  X  +•  + +  /X  X X  X  X  v  + + + \+ + -t•+ + +  X  X  X  X  X  X  X  X  x)  X  X  X X  >l  tt t t +  +  +  +  +  +  +  +  +  +  +1 +• + + + +  \+ + + -t•+  X  +  +  +  +J  2 5  300m A A A  Figure  3.1  Locations  of  diamond  drill  - 54 -  holes  sampled  A  for this  study.  1984) and 450  every  samples  were  alternate  we're t a k e n  collected  from  10 f t . i n t e r v a l  (Appendix  was  sampled;  a total  C ) . Wherever  possible  chip  outcrop within  a 50 f t . r a d i u s  of each  of  samples drill  site.  Precipitate main  each  were  creek;  taken  3.2.2  and  repeated  disc  sediment  samples  were  collected  from  mill.  pestle  and  perchloric nickel,  Preparation  stream  along  collected  c r u s h i n g and Precipitate mortar. acids  water  over  pH was  the e n t i r e several  length  weeks  determined  sediment of  from  using  liquid  samples  X-Ray  Fluorine  samples  samples  an.d c o p p e r , silver  Analysis  was  by h o t c o n c e n t r a t e d  and manganese  distribution  zinc,  were  elements  determined  by  extraction  of elements  nitric-  by f l a m e  determined  10 g p r e s s e d  on  powder  ion electrode  -  copper)  atomic  t h e same  after  fusion.  (particularly  55  agate  determined  used  mesh  ceramic  cadmium,  specific  t e c h n i q u e s were  -  100  lead,  were  f l u o r e s c e n c e (XRF) u s i n g was  to minus  h o m o g e n i z e d u s i n g an  molybdenum,  A). Major  reduced  i n a jaw c r u s h e r and  were  c a r b o n a t e / p o t a s s i urn n i t r a t e  Sequential  were  pulverizing  Digestion  (Appendix  by  and  sediment  absorption  sodium  were  At a l l l o c a t i o n s  cobalt,  pellets.  f t . intervals  the  solution.  Sample  Rock  a t 150  precipitates  locations.  indicator  by  stream  d r a i n a g e s on .the p r o p e r t y ( R e d a n d Pump C r e e k s ) . F i n e  samples  six  and  to study between m i n e r a l  a  Sequential Extraction Extraction 10%  Phases Dissolved  HCI Carbonates, adsorbed  Ammonium Oxalate Amorphous oxides KCI0 /HCI 3  Sulphides HNO^/HCIO^ (4:1) Silicates  Figure  3.2 S e q u e n t i a l  extraction  procedure  -.56-  f o rd r i l l  core  samples.  phases  i n r o c k s and  samples  i s summarized  extractions  used  Extract  solutions  iron  flame  by  3.2.3  Quality  determined Precision  on  i n Figure  3.1  were  The  procedure  ( d e t a i l s of are  the  detailed  for core  sequential  i n Appendix  A).  a n a l y s e d f o r c o p p e r , molybdenum, c a l c i u m  and  absorption.  Control  of  using  total  Table  precision  the method  e s t i m a t e s are  3.1.  Element Cu . Mo Pb Zn Ni Co Ag Mn F After  precipitates.  outcrop samples  atomic  Estimation  3.3  stream  f o r a l l g e o c h e m i c a l a n a l y s e s were  of Thompson  summarized  Analytical  and  i n Table  Precision  Precision  6  and  3.1.  n=  29)  1% 5% 15% 10% 10% 20% 10% 15% 20%  9  m e t h o d .of T h o m p s o n  1978).  Precision  Si0„ Al 0o Fe^O^ MgO CaO Na„0 K Ti0„ P 0 2 5 r  (1976,  (95% l e v e l ;  Oxide  15% 25% 30% 15% 20% 20% 35% 25% • 60%  Howarth  U  Howarth  (1976,  1978)  RESULTS  3.3.1  Geochemical  Major reflects  element the  Patterns  i n the Hypogene  distribution within  compositional  the hypogene  variations  -  57  Zone: Major  -  of  zone  Elements  strongly  t h e h o s t r o c k s ( F i g . 3.3)  12  13  12  74  11  12  11  72  10  11  10  70  9  10  9  8  9  8  8  7  68  < >  2  HORN \  | QMP  PBQP |,  %TiQ  HORN |  QMP  76  PBQP |  |  %CaO  HORN |  |  PBQP |  QMP  %MgO  3  QMP  2  HORN |<  %Fe 0 PBQP f  2  PBQP | HORN f  QMP  |  %SiQ  20  < > <  >  66  7  64  6  7  6  5  6  5  4  5  4  62 60  <  10 <  >  < >  58  3  4  3  < >  56  2 <  54  1  52  o  < > <  3  2  2  1 < >  1  F i g u r e 3.3 M a j o r e l e m e n t mineralized zone.  00  0  geochemistry  of  : Ii  rock  units  from  the  The  most  obvious  hornfelsed are  p a t t e r n i s the  volcanic rocks  c h a r a c t e r i z e d by  abundance Figure type  of  3.3  from  content  mafic  minerals  the  amount  concentrations calcite  Fe  the  the  phases  of  major  largely  in late  of  biotite  Distribution  monzonite  the  altered  s t o c k . The  former  reflect  variations  Variation stock  i n the  can  be  plagioclase the  major  of  rock  element  correlated  present .  presence  veins  f o r each  with  the  CaO  a n h y d r i t e , gypsum  ( H e b e r l e i n and  Godwin,  and  1984).  0 and K 0 r e f l e c t s h y d r o t h e r m a l alteration. 2 2 • A n o m a l o u s l y h i g h K 0 c o n c e n t r a t i o n s ( i . e . g r e a t e r t h a n 4.3% - f r o m 2 l o g p r o b a b i l i t y g r a p h s ) a r e a r r a n g e d i n an a n n u l a r z o n e t h a t corresponds (Figs. stock  1.3 with  influences  Na  to  areas  of  and  2.1).  Na  values  secondary  biotite  and  0 d i s t r i b u t i o n . The PBP u n i t 2 t h e o t h e r i n t r u s i v e p h a s e s and  than  higher  modal  orthoclase  0 i s c o n c e n t r a t e d towards the 2 d e c r e a s i n g g r a d u a l l y o u t w a r d s . Rock  Na  values  andesine).  of  quartz  element  the  and  hydrothermal  c o n t r a s t between  0 , TiO and MgO c o n t e n t s due t o an 2 3 2 ' ( h o r n b l e n d e , b i o t i t e and chlorite).  m i n e r a l i z e d zone.  within  relative  high  illustrates the  and  sharp  percentage  Highest  Na  of  plagioclase  0 values  occur  c e n t e r -of type  ( F i g . 1.3) this  (19%;  i n the  alteration  has  similarly higher  is attributed  oligoclase intrusive  the  to  a  to  breccia  pipe  2 south  of  the  3.3.2  Geochemical  Zonation demonstrated  stock.  P a t t e r n s i n the  of  t r a c e elements  by  defining  Hypogene  within  'anomalous'  -  59  the  Zone:  Trace  hypogene  zone  sub-populations  -  by  Elements  can  be  partioning  (on  rock  type  probability the  and  gr'aphs  'anomalous'  element (Fig. zone  alteration)  high  that  the  populations  high  s t r a d d l e s the concentrations  close  areas  Copper  grade  Table  3.2  having  1976).  and  On  a i d of  low  a cross  section  contact.  of  occur  away  element  A statistical  f o r copper  copper  cumulative,  populations  intrusive  a high  decreases  Trace  3.2.  population  greatest to  the  ( S i n c l a i r , 1974,  i s shown i n T a b l e  3.4),  with  forms  i n the  the  intrusive  Threshold  Cu Mo Zn Pb Ni Co Ag  300 102 88 23 21 16 2.31  XI  SI  for  each  the  deposit  this  zone  altered  of  annular the  hornfels  ratios  (Fig.  2.1).  contact.  p o p u l a t i o n s : hypogene  Element  summary  a prominent  Within  chalcopyrite/pyrite from  of  log  zone  X2  (n=  241)  S2  1252 1348 109 320 243 80 153 70 39 4 36 10 28 6 15 6 29 13 2 .,91 0..49 1 . 24  51 80 25 84 2 2 0  Thresholds determined by p r o b a b i l i t y g r a p h s ( S i n c l a i r , 1 9 7 4 ) . X I a n d X2 r e f e r t o t h e means o f t h e h i g h a n d l o w p o p u l a t i o n s , respectively. S I a n d S2 r e f e r t o t h e s t a n d a r d d e v i a t i o n s o f t h o s e p o p u l a t i o n s . A l l v a l u e s a r e i n p a r t s per m i l l i o n .  Molybdenum enclosed grades  more and  are  silver  i n an  the  copper  zone  found  at  are  anomaly  extensive zinc  occurs  within  distributions the  also  the  to  i s more  sub-populations  of  those  the of  restricted  (particularly form  zone  ( F i g . 2.1).  contact  similar  annular  to  the  distal  -  60  copper  south  haloes  -  entirely  molybdenum  Silver and  the of  is  Highest  stock.  and  that  and  molybdenum,  fluorine the  fluorine  anomaly  intrusion).  around  the  however  ore  is  Lead  shell.and  -Pb  Q. < O  -Zn -Ag -Mo  -Pb  -K  LU  LU  —Zn  LU  <D O 0. >I  o  Z —Mo  K  LU  -Ag -Cu -F  <  -Mo  0_ (0  -Pb  K  -Pb  -Zn  LU  z  Mo  -Cu  z  O DC  Pb  -Pb  -Ag -Cu  K  Pb  -Zn  Ag -Mo —Cu  -Pb -Zn  -Ag -Mo Cu  N  T  T.I, l |  v  1 '  F i g u r e 3.4 E l e m e n t z o n a t i o n i n t h e h y p o g e n e , s u p e r g e n e and capping zones a t the Berg d e p o s i t . Element l i n e s r e p r e s e n t d i s t r i b u t i o n o f a n o m a l o u s p o p u l a t i o n s ( T a b l e s 3.2 a n d 3.3) from p r o b a b i l i t y graphs.  -  61  -  leached the defined  a  second,  inside  3.3.3  poorly  the  developed  cop-per  persist  to  processes. maximum  anomalies  element  The  copper  zone  at  intrusive  are  the  absent  3.3.  with  from  Trace  element  contact,  leached  cap  T a b l e 3.1  are  largely  inter-element  for  by  populations:  Leached  3.3)  supergene  silver  zone  and  north  supergene  SI  Cap  Table  supergene  the  and  with  fluorine south  (n=98)  X2  S2  1000 60 36 . 10 0.39  700 39 18 5 0  ex p l a n a t i o n  r e s p e c t i v e l y . Although  retained  considerable  i n the  supergene  vertical  i n v e s t i g a t e d using  a  hypogene and  redistribution  sequential  geochemical  leached of  cap,  elements.  extraction  and  ratios .  sequential  partitioning  intrusive,  ( F i g . 3.4;  at  2300 390 170 61 590 235 17 ' 36 2.45 0.55  been  the  and  whereas  1610 90 209 21 0.60  patterns  silicate  the  Zone  i n the  Cu Mo Zn Pb Ag  intrusion,  The  becomes w i d e r  XI  been  within  modification  Threshold  the  has  little  patterns  Element  of  This  Supergene  zonation  surface  See  there.has  i n the  the  Table  sides  Patterns  trace  grades  i s developed  zone.  Geochemical  Primary  halo  of  e x t r a c t i o n technique  copper  minerals  to  be  between  carbonate,  studied.  -  ( F i g . 3.2) oxide,  When p l o t t e d on  62  -  allows-the sulphide a  cross  and section  of  F i g u r e 3.5 R e d i s t r i b u t i o n o f c o p p e r b e t w e e n c a r b o n a t e , oxide, s u l p h i d e and s i l i c a t e m i n e r a l s i n t h e h y p o g e n e , s u p e r g e n e and leached capping zones at the Berg d e p o s i t . S t r i p p l o t s d i s p l a y t o t a l copper ( d o t t e d s o l i d l i n e ) , s u l p h i d e c o p p e r ( s o l i d l i n e ) and c a r b o n a t e p l u s oxide copper ( d o t t e d l i n e ) . Shading o u t l i n e s the e n r i c h e d zone.  -  63  -  the  deposit. ( F i g . 3.5), the r e s u l t s  show t h a t  s u l p h i d e s (KC10 3 Nevertheless  I  extractable in  copper) are the p r i n c i p l e  some a r e a s  10%  HC1 e x t r a c t a b l e a n d ammonium near  extractable  copper,  supergene  addition, adjacent  085  zone  to mafic oxide  but nowhere Molybdenum  molybdenite zones. iron  reported  (SUS) t o form oxide  dikes  that  (Panteleyev,  species  Other  zones and  SOX c o p p e r  holes  zone. BRG DH078 a n d  exceed  SUS.  to copper  with  i n the hypogene  and s u p e r g e n e  i n h i g h l y o x i d i z e d areas  molybdenum  minerals  have  an i r o n - m o 1 y b d e n u m  Mariano,  1967) .  oxide  of elements  instance to TiO  spinel species  i s also  we h a v e  used  on t h e b a s i s  where  been  1 9 7 6 , 1981) and i n c l u d e s e v e r a l o x i d e s  unknown molybdenum  concentrations  i n KC10 - 3  zone. In  i n fault  in drill  distribution  i s widespread  are abundant.  In this  developed  shows a s i m i l a r  oxide  cut the m i n e r a l i z e d  on t h e s e c t i o n d o e s  hitherto  ratios.  a r e found  cross  (SOX) i s b e s t  Redistribution  by a d e c r e a s e  a supergene  minerals  as t h e dominant  (blanchardite;  e x t r a c t a b l e copper  i n d i c a t e s o x i d a t i o n i s o c c u r r i n g a t the top of  Ferrimo1ybdite  oxides  oxalate  the s u r f a c e ) , accompanied  supergene  Supergene  f o r copper.  (BRG DH078 a n d 0 8 5 : F i g . 2.1 a n d 3 . 5 ) a n i n c r e a s e i n  (especially  the  host  species  [FeMoO  ] and s i b o l a i t e ; 4 [MoO ] ( N o r t o n a n d 2 .  studied  using  the r a t i o  a  interelement  of t r a c e  element  that:  2 1)  TiO  i s primarily 2 rutile, ilmenite,  hosted  i n resistant  and m a g n e t i t e  -  64 -  minerals  and hence  such  as  i ti s particularly  resistant  to r e d i s t r i b u t i o n  2) C o n c e n t r a t i o n s  of TiO  during  weathering,  are reasonably  and  c o n s i s t e n t i n the  2 intrusion  (0.41%  + 0.15%) and t h e a l t e r e d  h o r n f e l s (0.91%  +  0.20%)  Results expressed  normalized  to the underlying  by t h e f o l l o w i n g  hypogene  zone, are  ratio:  x  x M/  H  (TiO )  M/ (Ti0 ) R  2  Where  "M"  leached  represents  capping  Table  the element  zone  3.4 T i O  of i n t e r e s t ,  a n d " h " .the h y p o g e n e  ratio  -z— Zone Cu  —  data  "x" the supergene  zone.  f o r diamond  d r i l l h o l e BRG  Mo  Pb  Zn  Ag  Mn  CAP  0.3  13.0  2 . 8.  0.7  11 .3  1 .3  SOX  4.2  10 . 2  4.6  1.8  5 .4  0.6  SUS  n . p . n . p . n . p . n . p ., n .P •  HYP  1.0  1.0  1.0  or  1 ..0  1.0  DH078  n .p . 1.0  A b b r e v i a t i o n s : CAP= l e a c h e d c a p , S0X= S u p e r g e n e oxide z o n e , SSX= S u p e r g e n e s u l p h i d e z o n e a n d HYP= H y p o g e n e z o n e , n.p.= z o n e n o t p r e s e n t .  There  i s considerable  three  samples  copper value  ranges i s used,  local  collected from  near  variation drill  in this  hole  BRG  r a t i o . . For example  DH078,  0.299 t o 0 . 3 3 6 . N e v e r t h e l e s s ,  consistent trends  emerge.  - 65 -  Average  in  the r a t i o f o r  when an ratios  average of l e s s  than  1.0,  therefore  and  values  BRG DH078 elements zones).  than  Table  (leached)  enrichment.  2 Zone  enrichment  ratio  Ferricretes show h i g h  Thus,  manganese  data  in drill  zone  at the surface.  f o r diamond  drill  hole  BRG  Zn  A8  Mn  CAP  n .p .  n .p .  n .p .  n .p .  n •P •  n .p .  SOX  4.2  2.8  3.6  14.0  1 .3  1 .6  SSX  1 . 2  0.8  0.6  1 . 7  1 .4  0.5  HYP  1.0  1.0  1.0  1 .0  1 .0  the capping  area  to the surface, a l l  Pb  2 4 5 , Ag 4, Mn  table, a l l  t a b l e i n an  Mo  values  hole  (SUS a n d SOX  Cu  samples  zone  are enriched. In  to the water  i s close  a  and z i n c a r e  l e a d and s i l v e r  zone  from  t h e water-  enrichment  3.5), close  are enriched  3.5 T i O  depleted  3.4), situated.above  but molybdenum,  ( F i g . 3.5; T a b l e  studied  has been  i n the supergene  n.p.=zone  from  1.0 i m p l y  ( F i g . 3.5; T a b l e  the supergene  elements  Zn  the element  I n t h e o v e r l y i n g CAP, c o p p e r ,  DH085  where  greater  that  are enriched  depleted BRG  imply  •1 . 0  DH085  not present.  taken  from  s e v e r a l l o c a t i o n s on t h e p r o p e r t y  f o r a l l elements  studied  155 and- F 4 8 0 ppm) are being  tied  suggesting  up w i t h  -  ( C u 9 5 0 , Mo  66 -  that  2250,  elements  Pb 3 7 7 , leached  the limonite minerals.  3.4  DISCUSSION  Trace  element  coincident  copper  accumulations  of  other  porphyry  Olade  and  differs silver  apparent  highly  and  are  leaching  considerable  well  silver. was lead  also and  deposits such  distal  e.g. as  patterns  except  ground only since  water,  the  Ely  This as  there  Enrichment  of by  molybdenum  zinc  ( i n the  i n outcrop  zones  1978)  capping  to  samples  is  chemical  weathering  as  oxidation  have  exceeded  copper,  i s surface molybdenum  Panteleyev  enrichment i n the  (1976,  is consistent  -  mechanical  manganese  with  67  -  Berg 1981) the  and of  still lows,  the  and  deposit.  erosion  (as  z i n c have  been  molybdenum,  lead  gossan and  a  topography of  by  elements  e s p e c i a l l y i n topographic  well  i t  leaching  Pleistocene)  rugged  has  zone.  despite  the  and  1976).  ( f o r the  reflects  78),  zinc  Gott,  due  patterns  1976; copper  leached  i n part  leaching  hole  the  Furthermore,  glaciation  or,  and  for  with  (Chaffee,  lead-zinc  of  relative  copper  and  (McCarthy  those  modified.  secondary  drill  reported  of  silver  Kalamazoo  with  reported  Chaffee,  lead  e l i m i n a t i o n of the  last  proportion  whereas  for  slightly  Where o x i d a t i o n and  depleted  the  zone,  distal  patterns  1973;  a s s o c i a t i o n of  with  more  to  Nash,  to  mechanical'  at  as  and  hypogene  and  similar  hypogene  sulphides.  case  are  p r i m a r i l y i n the  primary  the  amomalies  (Theodore The  i n the  i s enriched  e i t h e r as  rapid  zinc,  deposits  present  the  and  other  that,  acidic  studied)  for from  Comparing is  lead  as  patterns  molybdenum  deposits  zones  been . r e p o r t e d  where  and  F l e t c h e r , 1976).  molybdenum  This  distribution  and  leached  enrichment  presence  of  of  is  and cap  both  ferrimolybdite may  also  and p o s s i b l e  be i m m o b i l i z e d  plumbojarosite  in jarosite,  on t h e  prop er t y . S i l v e r  b u t t h i s ha s n o t  been  proven at  Berg.  Clastic initially  contain  associated be  material  with  incorporated  anomalous  into  oxide  limonite.  Molybdenum  oxide  gossan  fragments  acidic  ground  leaching a  sediments  may  be p r e s e n t  or' t o g e t h e r  with  and amorphous iron  waters  and manganese encountered  of several  or secondary  dikes)  should  elements  Thus,  copper can sulphides,  or associated  ferrimolybdite  lead  i n limonitic  and s i l v e r  precipitates.  oxides  neutral  which  Zinc  i s generally  p r e c i p i t a t e d where  surface  waters.  would  mo1ybdenum-1ead-si1ver-f1uorine  signature  i n rocks  probably  Continued result i n  at the surface  the deposit.  CONCLUSIONS  The  Trace  following conclusions  elements  form  c a n be made  distinct  annular  -  68 -  from  zones  as  with  as m o l y b d e n i t e ,  in relief  3.5  accompanied  oxide  the deposit  products.  as p r i m a r y (near  from  by r e d u c t i o n  above  1)  with  concentrations  and c a r b o n a t e s  minerals,  associated  derived  a v a r i e t y of weathering  secondary  or  i n the drainage  this  around  study  the i n t r u s i o n  within These  the  hypogene  zones  supergene  are  Copper  is primarily zones.  areas  intense  of  oxide  There  been  whereas  supergene Copper,  Zn,  Cu  Zn,  and  i n the  supergene  leached  i n the  supergene  i s shown  by  and  capping.  supergene  oxide  an  supergene  and  assemblages  increase  in  in  carbonate  copper. vertical  highly leached leached and  are  redistribution  areas  capping  Mn  from  molybdenite, sibolaite.  Pb  Ag  and  d e p o s i t . Cu  sulphides  deposit)  directly  of  leaching  h i g h l y mobile  in sulphides  considerable  Pb,  the  secondary the  hosted  the  by  Mo,  with  Ag  and  respect  depleted  i n the  to  of  elements  Pb  are  the  leached  hypogene cap  and  zone.  Mo,  draining  from  leaching  i n the  modified  being  Development  l e a c h i n g . In  concentrated zone,  Zinc  associated  has  during  slightly  i s removed  hypogene  and  only  processes.  environment  zone.  or  (as  Mn  can  are be  present  a result  associated with  solution.  of Zn  as  rapid and  be  present  f e r r i m o l y b d i t e or  as  oxides  Ag  are  associated with  i n the  detrital  creeks  primary  or  p h y s i c a l weathering  Mn  can  and  Mo  a l l anomalous  i n oxides as such  precipitated  detrital as  jarosite  blanchardite and  primary  sulphides . A highly leached Mo-Pb-Ag-F  deposit  s i g n a t u r e over  of  this  the  -  type  will  mineralized  69  -  of  show a s u r f a c e zone.  rock  and  CHAPTER  4.1  4 L E A C H I N G AND  SUPERGENE  ENRICHMENT  AT THE  BERG  DEPOSIT  INTRODUCTION  Previous processes  chapters  that  mineralization,  p r i m a r i l y have  are responsible alteration  deposit  and m o d i f i c a t i o n s  In  chapter  this  supergene  profiles  development  Hypogene blanket that  from  of these  three  of these  from  related  to the surface  than  of three  hypogene  by s u p e r g e n e  zone  (BRG DH076, 0 7 8 , 0 8 0 ; for  topographic  Fig.  c o n t r o l on  330 f t . A  and i t s t h i c k n e s s (Figs.  c r e s t s . On s t e e p  from  on v a l l e y  - 70 -  1981)  leached i s closely  3.5 a n d 4 . 5 ) . Maximum  hillsides  5 f t . ) or absent.  extensive  1967;Panteleyev,  over  recorded  t o 15- f t . w h i l e  processes.  c h a r a c t e r i s t i c s of  i s o v e r l a i n by a n  48 f t . t o  been  a t t h e Berg  i soutlined.  (Stewart,  topography  o f 75 f t . h a v e  to the ridge  the. o r d e r  holes  and a model  enrichment  overlies the enriched  close  drill  profiles  capping  thicknesses  patterns  patterns  m i n e r a l i z a t i o n a t Berg  i n thickness  with  f o r t h e development of  and g e o c h e m i c a l  i n detail  of supergene  varies  concerned  m i n e r a l o g i c a l and g e o c h e m i c a l  3.1.) a r e d e s c r i b e d the  been  drill  holes  on o r  t h e cap i s t h i n n e r , i n floors  i t i sthin  (less  ZONE  MINERALOGY PY, CP.Mo. GY.Cv Cc .09 .Mc.Tn .Cu . Fm.Li  0.  i  I  <  J_u.. — _ _ _ J _ L ' 4 —  *  X UJ O (/> QC UJ </> UJ  -  JJ_1  51 y  GYPSUM  ^ 1  Q. >1  F i g u r e 4.1 A s c h e m a t i c s u p e r g e n e p r o f i l e f o r t h e B e r g d e p o s i t illustrating the v e r t i c a l d i s t r i b u t i o n o f p r i m a r y and s e c o n d a r y m i n e r a l s . A b b r e v i a t i o n s a r e as f o l l o w s : CAP=leached c a p p i n g , SOX=supergene o x i d e z o n e , SUS=supergene s u l p h i d e z o n e , HYP=hypogene zone, R S E = r e s i d u a l supergene enrichment zone, ESE=enhanced supergene enrichment zone, C c = c h a l c o c i t e , C p = c h a l c o p y r i t e , Cu=native c o p p e r / c u p r i t e , Cv = c o v e l 1 i t e , Dg = d i g e n i t e , F m = f e r r i m o l y b d i t e , Gy=gypsum, L i = l i m o n i t e , M c = m a 1 a c h i t e / a z u r i t e , P y = p y r i t e , Tn = t e n o r i t e .  -  71  -  4.2  SUPERGENE  ZONATION  A generalized showing  distribution  illustrated and  vertical  hypogene  of  ground  gypsum  Three sulphide (CAP).  gypsum;  water  line  line  Each  zone  (Panteleyev,  zones  a supergene  become  sealed  a s t h e maximum- d e p t h Elevation  of the  topography.  have  oxide  i s characterized  i s sharp  1981; H e b e r l e i n et  hypogene m i n e r a l s .  surface  zone  fractures  i s interpreted  with  supergene  where  zone  minerals i s  of the supergene  the level  parallels  (SUS),  and hypogene  line'  level  interaction  distinct zone  marks  this  crudely  through the supergene  4 . 1 . The b a s e  by t h e 'gypsum  a l . , 1983). This by  of supergene  i n Figure  delineated  profile  been zone  identified:  a  supergene  (SOX) and a l e a c h e d  by a n a s s e m b l a g e  cap  of secondary  minerals .  a)  t h e SUS  chalcocite coatings  zone  i s characterized  (Panteleyev,  1981).  These  by c o v e l l i t e , minerals  on, or r e p l a c e m e n t s o f , hypogene  chalcopyrite) immediately  and as f r a c t u r e  below  the water  fillings.  table  digenite  and  o c c u r as s o o t y  sulphides  T h e SUS  (pyrite  zone,  and i s s u p e r i m p o s e d  black and  i s found onto  at or  hypogene  mineralization. b)  t h e SOX  zone,  though  the  t o p o f t h e SUS. T h i s  and  tenorite),  (brochanthite  not u n i v e r s a l l y  zone  i s typified  developed, i s present at  by c o p p e r  c a r b o n a t e s ( m a l a c h i t e , and a z u r i t e ) and c h a l c a n t h i t e )  m o s t w i d e s p r e a d SOX m i n e r a l  accompanied  i s cuprite  - 72 -  which  :  oxides  and  (cuprite  sulfates  by some l i m o n i t e . o c c u r s as s m a l l  The (100 to  500  u) e u h e d r a l  boxwork  cavities.  coatings rarely  Tenorite  as d i s s e m i n a t i o n s , b u t a r e most  mineralized  zone.  minerals  form  minerals  encountered  1981)  zone  species after  indigenous  native  abundant  down  In outcrop  hypogene  (fringing outcrops  dikes  that  hole  Other-  (Panteleyev,  to the deposit zone  and e x t e n d s  contacts.  by an a b u n d a n c e  of l i m o n i t e  minerals  f e r r i m o l y b d i t e and o t h e r  and s u l f a t e s ) t h a t  occur  unidentified  as boxwork  l i m o n i t e ) and as l a m i n a t e d  to b o t r y o i d a l coatings  environment  have  characterized  l i m o n i t e ; c f. Blanchard,  of supergene been  profiles  observed  fillings on  1968).  by d i f f e r e n t  f o r three  combinations geochemical  data  080  i n F i g . 3.1) r e p r e s e n t i n g i n Figures  r e l a t e d to  a t the Berg  geochemical  illustrated  fillings  Profiles  SUS) a n d by d i f f e r e n t  located  from  gradational  l i m o n i t e ) , as f r a c t u r e  types  these  with  jarosite,  (transported  SOX  BRG DH080  i n diameter. antlerite  on  crosscut  (indigenous  Supergene  Three  coatings  occur  1968).  to the enriched  sulphides  as  and a z u r i t e  to d r i l l  include:  a r e found  and/or  to mafic  up t o 5 mm  i s ubiquitous  oxides  Malachite  close  i n t h e SOX  hematite,  of i r o n  close  limonites i n  copper  fracture fillings  i s characterized  (goethite,  and  and r a r e  discrete pellets  t h e CAP z o n e  surface  This  4.2.1  granular  and d e l a f o s s i t e (Owens, c)  the  with  on f r a c t u r e s and i n b o x w o r k s .  minerals, the  crystals  diamond  of supergene  holes  Each i s zones  ( C A P , SOX  G e o l o g i c a l and (BRG D H 0 7 6 , 0 7 8 a n d  the supergene  3 . 2 , 3.3 a n d 3.4  - 73 -  deposit.  patterns.  drill  topographic  (GrafLog  profiles are  strip  plots).  For  each 1]  profile  and  visually  [columns figure.  or  with  of  the  BRG  of  DH076  Red  near  data  G-Scale for  are  of  [Appendix  copper,  displayed  as  strip  i n an  type  and  at. the  molybdenum,  ( F i g . 4.2)  Creek  surface  (Plates  sulphides  surface  oxidized present  1.1  are  in trace  and  on  4.1)  ore  minerals of  lead,  p l o t s on found  [column  left  zinc,  (pyrite  the silver,  the  right  i n the  three  coated to  Here  the  sulphides with  SUS  gypsum  53  f t . and  80  minerals  between  70  f t . and  80 f t .  very  factor  weak and [ e f ] of  silver  manganese  2)  strip  plots in Figure only  zinc  (ef=6+) are are  BRG  table  4.2  show  in  considerably  the  only  120  SUS.  In  enriched  partially These  are  f t . with of  highest SOX  enrichment  (enrichment  outcrop  while  and  copper  supergene  enrichment  at  profile  of  amounts  that  is  lead  copper,  ( e f = 5) zinc  and  depleted .  DH078  intersected  a  underlies  thin  a  2)  at  the  chalcocite)  minerals.  f t . Trace  d i s p l a y s any  appro.ximately  water  at  supergene  are  line  between  Element  the  d i g e n i t e and  concentrations occur  the  valley  c h a l c o p y r i t e ) . Leaching  hypogene  commonly amounts  and  incised  where  season).  (covellite,  i s weak and  and  collared  (depending  hypogene  and  B])  profiles  c o e x i s t i n g SUS  is  (rock  alteration  f i g u r e s . D e t a i l s of  contains  near  percentages  the  manganese  g e o l o g i c a l data  follow:  1) edge  and  document  estimated  Geochemical  side  holes  plots  2 to' 9]  fluorine hand  the  ( F i g . 4.3),  thick, (13  well  collared  developed  f t . ) CAP,  on  a  steep  supergene  characterized  -  74  -  south  facing  enrichment by  an  zone  abundance  slope, that of  PUCER 0EVEL0PM6NT LTD BE«G CU-MQ PORPWPV. PPQP£RTY  I p  :  § 11SI  I :« i'i 58  I  I  °»««i i  :>!!!!  • •  M3IIIII  5??  'a-  - i > 'ft  •  ±4* •  "3  illr  J-  •5?T  • I]  I 0-  - ±  = '  •  5  9a  I  • j • •  13  1 0-  US  rrtr » o o o o  •  3  >  Tit  •  3L  i I! I  I!!|  "{'" }  IN TERNA TIONAL  GEOSfSrEWS CORPORArION  GRAF.  I  °i388 I  •"I*""  1  LOG  F i g u r e 4.2 G r a f L o g s t r i p p l o t f o r t h e t o p 1 7 5 f t . o f BRG D H 0 7 6 . V e r t i c a l supergene zones a r e d e f i n e d d e f i n e d from g e o l o g i c a l data, i l l u s t r a t e d a t l e f t . G - S c a l e s y m b o l s ( A p p e n d i x B) i l l u s t r a t e m i n e r a l abundances. Geochemical data i s d i s p l a y e d as h i s t o g r a m s a t t h e r i g h t  - 75 -  limonite  and  a  lack  enrichment  occurs  Enrichment  zone  Supergene  Enrichment  enriched  i n copper  molybdenum  (ef=1.4).  In  secondary  two  F i g . 4.1) zone  the  2),  o v e r l y i n g CAP  considerably  enriched  4.3  but  upper  Residual  contiguous  show t h a t (ef=  i s only  zinc  Supergene Supergene  Enhanced  4.1)  molybdenum RSE  An  a lower  Fig.  i n Figure  the  minerals.  zones.  and  (ESE:  (ef=6),  (ef=  copper  distinct  patterns  (ef=1.2) while  (ef=2),  are  in  (RSE:  Geochemical  silver  of  2),  weakly  (ef=  1.2),  molybdenum copper,  the  zinc  ESE  (ef=1.5)  enriched lead  in  and  and  silver  manganese  and  copper  (ef=l.l)  ( e f = 1 0 ) and  zinc  is highly  silver (ef=6)  are  depleted.  3) thick  BRG (60  limonite amounts to  the  below  DH080  ft.) partially mantling  of  SUS  gypsum  line  present. (260  close  leached  partially  are  to  and  the  ridge  oxidized  decomposed Hypogene  zone  hypogene  sulphides  f t . ) . Limonite  crest, with  contains'a abundant  sulphides. increase  decreases  and  is  in  Small abundance  absent  66 f t .  Geochemical the  ( F i g . 4.4),  SUS  zone  patterns  with  limonite  maintain i s most  this  profile  copper, (ef=1.3),  ( e f = 1 . 5 ) d i s p l a y i n g weak (ef=2),  in  silver  enrichment.  hypogene  grades  Other  (ef=l)  abundant.  -  show l i t t l e  76  -  to  enrichment  ( e f = 1 . 3 ) and elements, the  fluorine  except  surface  in  where  silver  PLACER DEVELOPMENT LTD BERG CU MO PORPHYRY, PROPERTY, B.C. LE6END: KM-OI  DATE: M/02/14  i is  3  s :  •>ECT  HALE i * - n  -7-  Sal  n • - 3<  C D Z COUJ  71 mv>  I i II  •  ->  ».« - 3< > -> . -J  1  -3>».o - 3<  100  •  •  I  :1  o- 3* -J-  -y  too .  i  -ffIM.O-  DNE'  - 3"  ( <  i  5 ' 5  — — ISO o- ^—  •  11%  o o  a  I -  j  INTERNATIONAL  GEOSYSTEMS  CORPORATION  GRAF  »L O G  —  • - — - SIO 0-  PLACER DEVELOPMENT LTD BERG CU-MO PORPHYRY PROPERTY B.C. Q»T£;APRIL  j  i fjncnHoeo  fill  sou  i*  : -oo  -1> If  7  [J-  :i • • •  -  -  \r  •  j  • I  • )• )  z:  I -V  -J" 3  too 0- ^  if  :)• »>•• *  -u-ii-  [}-  • u• till  SSO 0-  ^  • ;7-  -3:r  i» 1 8  3  £ss  •3 ?M I  £8 8 1 | i  : »»ss ZT  I]  tzzi  °iI 5 8 8  IT  ZD "J  -Ji  i  I  s  T I]  :zi  :ZJ  ]  Jz  :i i zi z i  toe.o- -Zl  :z •  IT  •  • i  ID  :ZI Z)  13  :•  :z :zi  ZD  •  j 4-,-  -'.)'  -  8  • i "-P i i  !  SOD 0  • i • ]  LCBEM): KM-41  10/64  : « « * s»  Z) M  8 K  INTERNATIONAL GFOSYSTEMS CORPORATION  GRAF » LOG  8  i i  o  5S 8I 5  4.2.2  Leaching  Supergene using  and  Oxidation Indices  zones  i n Chapter  3 were  a sequential extraction.  define  oxidation  (0  ) and  Here  identified  the  same a p p r o a c h . i s  leaching indices  (L  i  of  values  i n the  copper  l e a c h i n g i n the  Leaching  depletion  at  extractions  hypogene  index the  zone. CAP  to  each  These  ratios  for different  =  100[  the  2)  indices  to  topographic  (Cu  t  are  intensity  environments.  amount  of  metal  value  copper  of  (HNO  copper  i s a measure  of  /.HC10 3 4 remaining  the  partitionin;  i of  a copper  expressed  between  oxide  and  sulphide minerals  c =  Cu  c=CAP, C u = c o p p e r ,  /  Cu  ox ox=10%HCl  and  is  ] sx  OX e x t r a c t a b l e copper, 4 i s e x p r e s s e d as a p e r c e n t a g e w i t h  sx=KC10 high  CAP  c  100[  i where:  i n the  as:  0  e x t r a c t a b l e copper. 0 3 i v a l u e s i n d i c a t i n g more i n t e n s e  -  of  )]  t=total  i s t h e r e f o r e the percentage i surface in a particular location.  : This  copper  t  L  0  total  q u a n t i f y the  )/  c = C A P , . h = h y p o g e n e , Cu = c o p p e r ,  Oxidation index  to  h (Cu  i  at  and  ): T h i s i s a measure of t h e i s u r f a c e and i s e x p r e s s e d by:  c  digestion).  other  (L  L  where:  ). These  used  i.  ratios  1)  specific  quantitatively-  79  p l u s NH  oxidation.  -  Table  4.1  D H 0 7 6 , 078 partially  summarizes  and. 0 8 0 .  the  Results  o x i d i z e d and  i n d i c e s f o r copper show t h a t  variably  in drill  a l l l o c a t i o n s are  leached.  0  values  holes at  suggest  BRG  least that  in  i spite the  of  the  copper  absence  i s present  extraction attacked  apparent  technique  by  a  of  i n these used  sulphide  SUS  from  minerals  removes  selective  CAP  (note  oxide KC10  the  at  that  copper  least  the  before  50%  of  sequential sulphides  extraction,  c_f. O l a d e  o x i d a t i o n has  occurred  are  and  3 Fletcher, CAP  of  grade  1976).  BRG  Maximum  DH078  remains  (steep  at  l e a c h i n g and hillside)  s u r f a c e . An  0  where  value  8%  of  of  50%  the  hypogene  implies that  in  the  copper half  of  i this  copper  remainder BRG  as  i s associated with microscopic  SUS  modest  35%  hypogene  50%  i s associated with  amounts  of  grade  l e a c h i n g and  remains  (as  minerals  minerals.  DH080 ( r i d g e c r e s t ) w h e r e  outcrop;  oxide  SUS  of  Leaching  the  oxide  ( l i m o n i t e s ) and i s at  hypogene  the  a minimum  grade  remains  at in  minerals.  BRG  DH076 d i s p l a y s  o x i d a t i o n i n the  CAP  where  and  hypogene  m i n e r a l s ) , 30%  17% in  of  the  oxide  minerals . Table  4.1  Leaching  Index  L. 0 1  _  4.3  I  and  oxidation indices  Drill  '  080 10% • 29%  hole  078 25% 83%  076 8% 15%  DISCUSSION  A model profiles  at  for Berg  topographic (and  other  control  i n the  d e p o s i t s ) must  -  80  -  development take  into  of  supergene  account  the  variable  nature  supergene 1982;  processes  to react  controlled 1)  air,  with  ( 1968)  sulphide  of o x i d a t i o n . S t u d i e s and o t h e r s  shown  that  minerals  of  (cf . Anderson,  the a b i l i t y  i n t h e zone  of  of o x i d a t i o n  by:  and o t h e r  surface  the abundance  fractures  zone  1960) have  fracture permeability  rain 2)  surface  by B l a n c h a r d  Emmons, 1 9 1 7 ; S a t o ,  groundwater is  of the near  that water  of s u l p h i d e  (as i s t y p i c a l  restricts  t h e f r e e movement o f  to the water minerals,  f o r hypogene  table,  particularly  along  m i n e r a l i z a t i o n ) over  a large  area, 3)  removal  otherwise  each  shield  reactivity  4)  temperature o  10  depth  6)  climate .  At  Berg  assumed  table,  of the w a l l  i s approximately  rocks, doubled  w i t h i n the temperature  with  range  and  of the above  the purpose  f a c t o r s c a n be c o n s i d e r e d  of t h i s  intensity,  surface  discussion. Wall  difficult  rock  t o be  reactivity i s  are quartz to quantify  and i s high  (> 50 f r a c t u r e s p e r m o f d r i l l  of ground  constant  gangue m i n e r a l s  although  environment  2.1). Temperature to remain  would  1968),  Fracture  the near  that  further oxidation,  ability  activity  t o be l o w a s - the_ d o m i n a n t  feldspar.  assumed  from  i n temperature  to water  three  sulphides  (chemical  (Blanchard,  5)  of o x i d a t i o n products  or n e u t r a l i z i n g  C increase  uniform'for  Fig.  fresh  3)  likely  in  by f l u s h i n g  water  throughout  - 81 -  (and hence t h e summer  core;  reactivity) i s season.  Figure deposit line  4.5  i s a schematic  ( F i g2 . 1 ) . Supergene  (GL) and i n t e r p r e t e d  approximate controls  depth  water  table  potential  environment  Partial  profiles  leaching  of part  with  (WT) l e v e l s  (derived  ground-waters  non-saturation  above,  of ground  and o x i d a t i o n  (stippled)  downhill  leaving  slowly  under  mantles  are observed  Periodic  recharge  oxidation surfaces  zone  waters  being  also  leaching  from  Copper  ground-waters  continually  derived  zone  oxidation  (solid  relatively  products build  from  Oxide this  up a  (limonite) environment.  accelerates  p r o d u c t s and e x p o s i n g  i n the weakly from  of fractures a i r  oxidize  oxidation. grains  top  migration  t h e zone  by m e t e o r i c w a t e r s  developed  the downhill  arrows)  rather  than  fresh  supergene. migration  of  vertical  table.  fillings  i n the h i l l s i d e  ( L =8%) s u g g e s t i flushed  oxidation  from  sulphides  further  c a n be d e r i v e d  fracture  about t h e  f o r each  by r a p i d  and o x i d a t i o n  sulphide  soluble  to the water  Limonite intense  of t h i s  for oxidation.  bearing  migration  retards  on m o s t  by l e a c h i n g  enrichment metal  conditions, that  conclusions  a l l but the smallest  f o r much o f t h e t i m e . H y p o g e n e  mantle  from t h e  o f t h e CAP a t t h e r i d g e  filled  protective  gypsum  c a n be made.  (broken arrows)  these  observed  B e a r i n g i n mind t h e  (BRG D H 0 8 0 ; L = 5 0 % , 0 = 2 9 % ) c a n be e x p l a i n e d i i of  of the Berg  are plotted  processes l i s t e d  and l e a c h i n g  topographic  section  o f SUS m i n e r a l i z a t i o n ) .  on o x i d a t i o n  oxidation  cross  that  by a c i d i c  uphill)  and  t h e n o n - s a t u r a t e d zone i s  ground  and t h a t  - 82 -  environment  waters  fractures  (sulphuric  acid  a r e wet most o f  the  time. Contribution  meteoric  waters  as  runoff.  The  is  suggested  t o and  i s minimal presence  by  an  0  dilution  on  of  of  the  the h i l l s i d e  only  v a l u e of  small 83%  ground-water  as  most w a t e r  amounts  i n the  of  CAP  copper  a t BRG  by  i s removed as  sulphide  DH078.  The  i shallow  depth  wasting) table.  i s keeping  SOX  indicates not  of w a t e r  that  by  at  intermittent  to  the  Berg  this  1976).  the  leaching  original  and  SUS  h a t c h i n g ) on  SUS  has  be  a regional  Development  of  the  (WT1  enrichment  and  (WT2;  the  copper  F i g . 4.1,  fine  DH078  phenomenon  (cf .  This  this  in a  zone  contributes  location  portion  is  easily  level  i n t h e ESE cross  water  SOX  table  upper  (mass  o c c u r r e d . As  i s more  at  the  i n BRG  F i g . 4.1).  observed  oxidizing of  SOX  i n water  t o WT2;  erosion  m i g r a t i o n , of  i n water, t a b l e  redeposition  level  mechanical  cannot  saturation  periodically  that  downward  (vertical  strong- supergene  table  with  a seasonal fluctuation  of  water  implies  a r e c e n t drop  Godwin,  explained  pace  overprinting  widespread  Casino:  table  of  by  the  at the  lower,  hatching; F i g .  4.5).  Coexistence  of  hypogene  and  SUS  minerals,  low  L  and  0  i (8 and the is  15%  respectively)  valley at  the  floor surface  ground-waters form SUS  thick  Development removal  of  ( F i g . 4.5;  ferricrete  of SUS  presence  Plate  surface  4.1)  and  d e p o s i t e d onto  mechanical  zone  erosion.  -  83  -  s p r i n g s , and  suggest  deposit  freshly  enriched  of  acidic  p l a t f o r m s i n the  a strongly by  the  i n BRG' D H 0 7 6 . H e r e  emerge a t  m i n e r a l s are  and  that  metal  at.  table  bearing  floors.  exposed  seepages  the water  limonite  valley  values i  m i n e r a l s to Below  hypogene  i s prevented  by  surface  sulphides. constant  076  F i g u r e 4.5 A s c h e m a t i c c r o s s s e c t i o n o f t h e B e r g d e p o s i t i l l u s t r a t i n g the r e l a t i o n s h i p between supergene zones, water table (WT), gypsum l i n e ( G L ) and t o p o g r a p h y . A r r o w s i n d i c a t e t h e p r o b a b l e p a t h of m i g r a t i n g ground water as i t t r a v e l s from h i l l top to v a l l e y floor .  -  84  -  4.4  CONCLUSIONS  Although conclusions the  a limited below  type.and  1) Py/Cp  1981:  These  Supergene ratios  intensity  (<  Figures  hypogene  24  water  table  with  the  water  table  and  t h e CAP  3 ) The  relationship and  exists  with  a r e a s o f maximum contact:  see  with  low  Panteleyev,  represents  t h e maximum  depth  supergene  zone  can  zones  zone of  between  fracture  s e p a r a t e s supergene  a zone  that  o c c u r s a t and  groundwater  i s d e v e l o p e d i n an  In  be  -  85  of  above  from  into related  the water SOX,  of i n t e r m i t t e n t  unsaturated  to  found  above  saturation  where m e c h a n i c a l  -  In t h i s  and  zone.  more r a p i d l y  weak.  the  table  developed i s dependent  floors  creeks i s proceeding development i s  below  saturation.  pro f i l e v a i l ey  divided  are s p a t i a l l y  i s d e v e l o p e d i n a zone  supergene  zones  line  SUS  the  topographic  This  distinct  study  F i g 2.4).  (GL)  environment.  down c u t t i n g  leaching,  line  The  zone  in this  follows:  type of supergene  topographic by  and. 2 5 ;  (WT).  coincides  used  profile  to the i n t r u s i v e  penetration.  mineralogically  been  a close  supergene  coincide  close  below.  has  enrichment, i s b e s t d e v e l o p e d where  gypsum  groundwater  of  a r e as  3:1)  (i.e.  2 ) The  suggest that  intensity  environment.  d a t a base  on erosion  than o x i d a t i o n environment  and  P l a t e 4.1 V i e w t o w a r d s t h e h e a d w a t e r s o f Red C r e e k . N o t e t h e s t r o n g l y d e v e l o p e d g o s s a n ; y e l l o w a r e a s a r e j a r o s i t i c and o v e r l i e the p o t e n t i a l o r e b o d y . A c t i v e p r e c i p i t a t i o n of f e r r i c r e t e s i n c r e e k beds i n d i c a t e s t h a t l e a c h i n g p r o c e s s e s a r e a c t i v e t o d a y .  -  86  -  hypogene or  sulphides  without  chemical  remain,  secondary  weathering  weathering  SUS  albeit  minerals.  i s proceeding  to produce  a thick  mineralization.  Seasonal  part  at the steep  to  o f t h e SUS  a SOX  water  that  more  table  rapidly capping  crest than  mechanical  underlain  environment  with  environment  f l u c t u a t i o n causes  hillside  table  development movements  5) M a l a c h i t e / a z u r i t e dikes  In the ridge  leached  water  a l t e r e d , at surface  by weak the  t o become  SUS  upper oxidized  assemblage.  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G e o l o g i c a l S u r v e y o f C a n a d a . , o p e n f i l e map  -  93  -  ( 9 3 E) 708.  map  APPENDIX ANALYTICAL  A  TECHNIQUES  - 93a  -  SUMMARY  Drill  BRG  samples  hole  SAMPLES  COLLECTED  Depth  Samples  DH021  522'  24  BRG DH025  446"  15  BRG  452"'  21  BRG DH068  363'  16  BRG DH069  601'  24  BRG  DH076  697'  31  BRG DH078  1001'  49  DH080  407'  20  BRG DH082  . 657'  32  BRG DH085  978'  46  BRG  Other  OF  DH026  BRG  DH088  1002'  49  BRG  DH089  487'  23  BRG DH092  1997'  70  collected:  Duplicate  samples  70  S t r e a m "sedimerut Stream  23  precipitate  7  Outcro p  40  Ferr i c r e t e  ]_ TOTAL  597  -  94 -  SEQUENTIAL  EXTRACTION  - CORE  SAMPLES  S t a g e A. 1) W e i g h  o u t 0.2 g r a m s  2) L e a c h  i n 20 m l o f 1 0 % HC1 i n u l t r a s o n i c  3) C e n t r i f u g e  Stage  and decant  sample. bath  f o r 30 m i n u t e s .  aliquot.  B  1) D i s s o l v e grams  2) L e a c h for  24.9 grams  of o x a l i c  adjust  o f ammonium o x a l a t e  acid  (dihydrate)  (monohydride)  in 1 litre  and 12.6  of d i s t i l l e d  water;  pH t o 3 . 5 . residue  from  Stage  A i n 20 m l o f s o l u t i o n  while  shaking  12 h o u r s .  3) C e n t r i f u g e  Stage  of  and decant  aliquot.  C  1) A d d 0.4 g r a m s HN0 3 2) L e a c h  of potassium  chlorate,  0.5 ml o f c o n c e n t r a t e d  a n d 4.0 m l o f c o n c e n t r a t e d HC1 t o r e s i d u e f r o m o sample  f o r 2 hours  3) Add 15.5 ml o f d i s t i l l e d 4) C e n t r i f u g e  and decant  i n hot a i r bath water  to bring  Stage  B.  (80 C ) . final  volume  t o 20 m l .  aliquot.  S t a g e J2 1) A d d 2 m l o f HnO /HC10 ( 4 : 1 ) t o r e s i d u e 3 4 in hot a i r bath. 2) L e a c h of  with  2.5 m l o f 6 M H C 1 ; b r i n g  distilled  water.  - 95 -  and e v a p o r a t e  to dryness  t o 10 m l by' a d d i n g  7.5 m l  SEQUENTIAL  EXTRACTION  - SURFACE  SAMPLES  STAGE A 1) W e i g h  o u t 0.2 g r a m s  2) L e a c h  with  of sample. -  10 m l o f 4 M HC1 w h i l e  i n ultrasonic  bath  f o r2  hours .  3) C e n t r i f u g e - a n d d e c a n t  aliquot.  S t a g e B_ 1) A d d 0.2 g r a m s  ( K C 1 0 ) , 2 ml o f 3 c o n c e n t r a t e d HC1 a n d 0.25 m l o f c o n c e n t r a t e d HNO . o 3 2) L e a c h s a m p l e i n h o t a i r b a t h f o r 2 h o u r s ( 8 0 C ) . 3 ) A d d 7.5 m l o f d i s t i l l e d w a t e r t o b r i n g f i n a l v o l u m e t o 10 m l . 4) C e n t r i f u g e  of potassium chlorate  and d e c a n t .  S t a g e C_  1) A d d 2 m l o f HNO 2) E v a p o r a t e 3) L e a c h  with  /HC10 ( 4 : 1 ) t o r e s i d u e 3 4 to dryness i n hot a i r bath. 2.5 m l o f 6 M HC1 a n d warm  4 ) A d d 7.5 m l o f d i s t i l l e d  water  to bring  - 96 -  from  Stage  f o r 1 hour. up t o 10 m l .  B.  .OPERATING  Element-  CONDITIONS  Slit  Scale  FOR  ( u ) Ma  TECKTRON  VARIAN  Wavelength  AAS  N 0 # Ai r 2  C H 2 2  Cu  Normal  50  3  3 2 4 7 .5  No  20  2.5  Ca  Normal  100  5  4 2 2 6 .0  Yes  20  a.r .  Fe  Normal  50  5  3719.0  No  20  2.5  K  Normal  200  5  7 6 6 4 .0  No  20  2.5  Na  Normal  100  5  5890.0  No  20  2.5  Zn  Normal  100  6  2 1 3 8 .0  No  20  2. 5  Mo  Expanded  100  5  3 1 3 2 .6  Yes  20  + Acetylene  gas used  as  required.  # Air  flow  Burner  rate  (  rotated.  - 97 -  /second)  -  STANDARD  ANALYTICAL  Element  Units  Mo  ppm  Cu  ppm  Zn  ppm  Pb  ppm  Cd  ppm  Ni  ppm  Co  ppm  Ag  ppm  F  ppm  METHODS  USED BY P L A C E R  Digestion  Time  Range  4 hrs  1- 1 0 0 0  AAS  4 hr s  2- 4 0 0 0  AAS  4 hr s  2- 3 0 0 0  AAS  4 hr s  2- 3 0 0 0  AAS-bkg  4 hr s  0. 2 - 2 0 0 A A S - b k g  4 hr s  2- 2000  AAS  4 hr s  2- 2 0 0 0  AAS  4 hrs  0. 2-20  AAS-bkg  30mi n  40 - 4 0 0 0  C HNO /HC10 3 4 C HNO /HC10 3 4 C HNO /HC10 3 4 C HNO /HC10 3 4 C HNO /HC10 3 4 C HNO /HCLO 3 4 ,C HNO /HC10 3 4 C HNO /HC10 <a 3 4 Na CO /KNO F 2 3 3  DEVELOPMENT  Method  #  +  @  Atomic  Absorption  Spectrometry.  Atomic  Absorption  with  Specific Na 2  background c o r r e c t i o n .  Ion Electrode.  CO /KNO 3 3  Fusion  -  98 -  SIE  #  LTD.  XRF  OPERATING  C O N D I T I O N S - MAJOR  ELEMENT L I N E TARGET C R Y S T A L  Kv/Ma COLL  AND  TRACE  ELEMENTS  COUNT VAC G A I N  WIN  LL  TIME  Si  K  Cr  PET  50/40  F  F  ON  128  700  150  10  Al  K  Cr  PET  50/40  C  F  ON  128  700  150  10  Fe  K  Cr  LIF200  50/35  F  F  ON  128  700  150  10  Ca  K  Cr  LIF200  50/16  F  F  ON  128  700  150  10  Mg .  K  Cr  TLAP  50/40  C  F  ON  128  47 0 150  10  K  K  Cr  LIF200  50/35  F  F  ON  128  700  150  10  Na  K  Cr  TLAP  50/40  C  F  ON  128  700  150  10  Ti  K  Cr  LIF200  50/35  F  F  ON  128  700  150  10  P  K  Cr  PET  50/40  C  F  ON  64 280  150  10  ELEMENT  PEAK  Si  109 . 14  113 . 30  Al  145 . 19  139 .00  57 .54  56 .00  Ca  113 . 17  110 .40  Mg  45 . 21  Fe.  K  ( 2 0 ) BKG  136 . 75  •  44 . 00 132 .15  Na  55 . 20  53 . 30  Ti  86 . 20  91 .00  P  89 . 61  92 .60  - 99 -  APPENDIX B 1 GEOCODER: A L i s t  1.  GEOCODER  of symbols  and codes  a n d GEOLOG a r e t r a d e m a r k s  Corporation. - 100 -  used  i n GEOLOG  of I n t e r n a t i o n a l  Geosystems  SYSTEM  -101-  International G e o a y a t e m s C o r p o r a t i o n U N I Q U E ID OF P R O J E C T DRILL H O / 4v F L A G S P E C OR SUB-PROJECT IX PRE-f 1 0 D E iN 6 B 0 2 Identity I < Dat a iP R J  a  s  Survey Data  Upper G eod  Tier a t a  Lower!n G eod a t e  s-  /  L  ||  A-  R  O  M  -  1  1 II I 1  T  O  -  N i  S i  HFr  T  'TP A V E R S E  NUMBER  y PE  u  5 T O T A L  1 1 II  1 1  1  R E C O V E R Y  1  SIZE OF CORE on H O L E •  I  1  N 1  ROCK  1  T M 1  0 L C> M O N T H  F. TRUf N  J  hi T M  2  G  CS  E  D  A S S T BY  B V  OR  D R 1 L L E 1 L L E RIS) M O N T H  1Y 0  TTT  M 1  1  T X 1  TX  |  ^ * t  2  1  T O T A L = T D . A Z M . V - A N G . N » E • EL  HASH  "oV»  l-l 0  1  1  V - A N G  FF C F  F  1 1  s'MI  R,  B1  I I|  t 1  N  O  R 1  R  on  Y 1  1  T  H  I  SURVEYED|CO-OBD BY 1 SY S T E M  N  G  1  1  STRIKE A Z M  D I I STRUC2 I D  or  A 0  PLUNGE  P  z  1  :t  J  , '  i w i T B 1 1  G R I D  |  C)  R  a i^i i ,  I 1 1DIPj to1Rt. 1 r  STRUCt I  OR 1L L I N G T1 M E -HRS  R I G T Y P E  R  \ P  — 1 — p h i  ¥ 1 CLOCKWS  A ZM  D1 E P T H / L E N G T H  T-MODL^  E  G  0  1  I  E  A  1  C Y  A Z I M U T H  T 1  S  T  cB  1 • 1  I  N  MG  1 1  S 1  P A G E  U 1  G  8 1  •  .  iH XX  R  1  V i s !  1  P  1 IU P Y  E  O  1  L  t t r n C P  E  1  V  IT  J A  1 T  E  1  I  Stl ires YY  G L  C 0  1  T  0 F >  j l  1  N  SI FA  .  1  B  H  Mh A R Y  Al Mz  b c  e 1  t n  !  1  r  1  a  JJ^ d  I 1 1 | I j 1 I ] 1 1 1 11 1 1 | | | o1 f||L |. r,!„„,•,., R • c o'v. 1.1 I.I 1 1 1 1 I I I 1 1 1 11 1 i 1 1 1 H w )W E NVIRHow Ami HowAmt J O I F > to Rt Unll o 1 / > M o r-4F . X T 1 • 1 2R O D P E O M 2 TX4 TX 3 SR P-N s % A Z M P R MO S L 1 2 L A G 1 roc* Ri B 2 Ffl r m 'n _L ^ H IJ"' iPr* K F M U C L E P H E /»>« «*«£ 1 M 2 ... A 1 1 1 II 1 > U " 1 1 9 1 ROD 6 I 21 i n 1 L 112 1 1 J 1 1 i .1 ) 6 7 8 41115 1 17 ie | 10 19 20 2S S1=22 123 24 25 10 31 .12 33 M .55 37A ?3H '9 40 .] 1 4 24A 34 4'15 4 0'I 7 48 49A 4 51 52 5 154 55 35 Lii_7 5059 60 61A 662 63 64 65 66 67A 76H 63 70 71 72 73A a74 175 76 77 78 79A 80 RECOVERY S a m p / e S e n a l No9 3 A 5 SS f From SS It In S S it From S S H H A S H T O T A L IhOn S rVo.P'oupa r P s s /I lo SS t r • 0 m SS It -•It < * » r Flig-COU. I « m FIIB or Fl»g C=oC' O2Mf a oBi 8 il= * . SMAX Or U IN To s sA 7HJ From d*tln»o ^FItg,Rnn, « n f* * n * no. Ot - PP #. 0 2 3 4 e 7 5 SN 9  NI AIM S I S I L 2 ON E F  A  J  HORIZON F L A G  //-  .t  F  TUF IN'G PT =Coilar  LE  1  i 1 L i  m n o 1 2  — ——  ....  —  ._.  ——  --  ——  ....  1  —  ——  —  -  1'  ....  ——  -  ....  -  ———  _ .  i  ——  ——  — —  -  I. . 1 j  --  —  ~  — —  ; —  — — \"  ——  —  —  —  —  —  !  ....  —  —  —  !  '  i  ^-  -- - -  ————  ——  J::  11  -  1  1  ..  1 1  -  —  ! .  <3 10  -  —  I . i ' , -.  ....  . ;  15  —— — — _..  ——— _  —  17 IS I'J  —  20 21  --  i  1_2_ 13  16  —  I '• • ;  _.!-..  —  1-1  !  ......  — ——  —  ...  f'  7  —  —  --  _— — —— 1  |  -  —  [  --  ————  6  8  il  ....  ...  -  ———  -  —  ——  1 IM  5  — -  -  "-  ...  1  j L  4 ...  j  1  —  3  22  —  • 23  i  2-1  25  ——_  26 27  -  —  28 29 30 31 32 33 34 35 36 37  V !  /  3 4 5 6 7.  2  4 5 6 V 8 9 10 1 11 21 11-1 15 1G 17 Ifl 1 920 21 22 2 J 2-1 15 no 2 72'3 29 30 31 32 3 3 i-1 2 -Two S = Alpha S  I 35 Kj| .17 IB ?  -  S e v e  38  40 4 1. 4 243 44 4 54 64 748 49 50 51 52 53 54 55 ',6 57 58 59 60 61 62 n I o, i = A l p h a I 0 = Alpha O  64 •")5 66 67 68 69 70 7 172 7 374 75 76 77 78 79 Alpha Z  oo  o O  FAssgn Value  Scale Value  55+ 45  X 9 8 7  36  28 21 15 10  o <  •  n o t n o T  a it  o 3  < •3 0 0  c  •  3  o ro  6  •5 4  6  3  3  2 1 0  . 1 0  SCALE  Description shattered extremely well fractured very well fractured well fractured f a i r l y well fractured moderately fractured f a i r l y l i g h t l y fractured l i g h t l y fractured very l i g h t l y fractured s l i g h t l y fractured unfractured  i  NOTE: It can be seen that the assigned value of each scale value i s the sum of the scale values from 0; for instance, the assigned value of scale 2 = 3 = 0 + 1 + 2 and the assigned value of scale 3=6 = 0 + 1 + 2 + 3 , and so on.  S C A L E A 1-CSAJUCTBR  PERCENTAGE G - S C A L E  the e s t i m a t e d percentage mineral  of  possible  diagnostic  interval-by-interval, ed r o c k  type present  To s t a r t up t o  lOOt,  with,  or'the  for  eral  X For  percentage  one-third  erisk,  * ,  above  of  the s t a r  ) -  cause  > .3t,  It,  also  ally  above  and b e l o w  and t h e a l n u s  for  other  the  sign,  a dot or  useful  estimate  like  these -  "  X  parameters,  each  associat-  to p r i n c i p a l  —  'ALE iLUE  alteration  ten percent  prevail  1 -  one.  over,  k  101,  2 •  90% and t h e Roman Num-  impossible,  lot,  we s t a r t  point,  the  two  is,  because  -031. St  And,  than,  ( •  .It,  . 1 < -3t.  Finally,  with by  -3t.  of  the  which i s Again  present,  0 • nil slash,  value  having  ast-  right  appropriate  sign,  of  "  like  •  the  2.5t  m  the  . •  O.Ot.  • and  .01t Two  / • present .07t,  an a s s i g n e d  and  but  the  value  of  ASSIGNED VALUE  loot  R A N  G E  E s s e n t i a l l y 1001  DECODED 2-DIGIT FORM Ut  90  85 t o  99  90  80  75 t o  <8S  80  70  65 t o  <75  70  60  55 t o  <6S  60  SO  45 t o  • 55  50  40  35 t o  «45  40  30  25 t o  OS  30  20  15 t o  <25  20  10  7 to  <15  10  5  3 to  < 7  51  2 to  2.5  < 3  2+  1  .5  to  < 2  It  •  .3  .2  to  <.5  .3  (  .1  -  .03  .  .01  0  0  /  .07  7  0  be-  symmetric-  a b o v e and b e l o w  by t h e  h a v i n g an a s s i g n e d  the  ones  the p l u s  course,  the  Symmetric-  and the p e r i o d o r d o t ,  are represented  7 * possibly  * •  'bent'  a greater  bracket,  off  represented  that  b e n t ones are  • for  trace.  values  question nark,  * are  appropriate  the e q u a l s i g n ,  just  addition  9 -  the G - S c a l e ;  and t h e l e f t  than,  are  or other  amounts  801,  a percentage of  which i s  less  -  B -  amounts b e l o w  and b e l o w  bracket, It  or  loot.  value,  ally  in  relationships to  r e c o r d i n g o n GEOFORM  importance,  percentage  the o b v i o u s  3 • 301 and s o o n ,  for  any o r e - t y p e  estimated percent of  i n an i n t e r v a l  20%,  10 -  presence of  .OS t o <.2  .1  . o 2 t o ».0S  03  T r a c e • «.02  01  N i l , Absent „ . Estimate " fmpossible Possibly Present  00  P r e  n  07 77  Ot:  NOTE IN PARTICULAR I) chat Uw I 1 ) I . u t u order of u j n i c u d t apart/ 1) that the • • - ere elto en order of ntgnl tude 'pert/ 3) chat the • ) • t ere a n u l t i p l a ot 1 apart; and 4) that Uw 8 4 3 1 - 4 are a n i l t i p l * of 3 epert. Beceuee ot the considereble separation between thete tcele v a l u t a , the G-Scele it a powerful ettimeting tool it eught be difficult to d i s t i n yuijrt between ttu .1 end .4% but with a l i t t l e M t of p r a c t i c e i t should not be too herd to d i s t i n g u i s h betveen .3 end J t i m s . J • 1».  H-  HOW  OR  SCALE  B-SC A LE  MODE Sym-  bol  B - S C A I< E OCCURRENCE  OF  DFT.RFE  0  F  1 3 "  PERVAS-  t\ -  IVE-  5 -  I NESS  6 -  I  INCREAS-  INC  81.050  2 -  7  'HOW' j ^ "  D e s c r i p t i o n  D e s c r i p t i o n  A (unyijdaloids,cavity f U l j B Blebs I breccia f i l l i n g * Amygdaloids (A), minor Hacroveins(>) C Coatings £ e n c r u s t a t i o n s and/or s c a t t e r e d C r y s t a l s ID) • clasts D Disseminations I s e a t . x ' l s E Envelopes Hacroveins(>) and Veins(V) F Framework c r y s t a l ! G Gouge Veins(V) and f *../ n „H Halt-s Da^ticnite.Y, { ^ « ^ I eyas, augan J interstitial K stocKworK Veins (V), and/or o c c a s i o n a l Envelopes(E) L Laminaeions/beddad M Hassiva N Nodules V e i n s ( V ) , and/or abundant Envelopes(E) 0 spots P Pervasive 1 , 0 patches, as i n Q u i l t s Pervasive (P) or 1 uss I V e i n s (V) ,Hicroveins(<) R Rosettes ( x ' l c l u s t e r s S Selvages Disseminations(D)J THAM \ Selvages(S),Envelopes(E) $ Sheeting T s T a i n i n g s , as i n T a r n i s h I CR£A- l U eU-hedral c r y s t a l s T V Veins m > nvacrovelns I THAM I < microveins,frac f i l l L n g s Pervasive(P) or D i s s e m i n a t i o n s ( D ) , V e i n s ( V ) , W boxworx Microveins(<).Selvages(S) I Envelopes(E) X Massive and/or lairv^na^ed^/ with mjch B r e c c i a f i l l i n g d ) , StocKworK(K) Y dalmationita and/or Sheeting(S) Z f r e s h . prkm*ry rock KJSsive(M) and/or Lamina ted/Bedded (L) fx lot  0 - F r e s h , prirtary r c c M Z ) , _ A "  O R  C r <  U  D  (  •  ltza)  Q  )  i  n  "  "  ? "\  Intarnattonal Oaoayatama Corporation  -10*+-  Vinoouvir,  Canada  ,  g  GEOLOG" SYSTEM  GRAIN  International Qeoayetemt C o r p o r a t i o n  1 GNEOUS, MCTAMiRPHlC i  RANGE  Classy  2  ASSGH SYM<««W GENERAL VORKSm 1.SSGN VALUE BOd MR DETAIL WORK* >BQL ^ L U E mm .003 .0OJ CLAY SIZE m •  CHARACTERISTICS  VOLCANICLASTICS  A  .008  V . F I N E SILT FINE  grained  .03  (aphanitic)  .12  SILT  MEDIUM S I L T COARSE SILT V . F I N E SAND  Pine  FINE  grained  MEDIUM SAND  2°-  .177  SAND  coarse  . 707  COARSE SAND 1-  Medium grained ( g r a n u l a r )  GRIT  GRANULE V.SrtALL PEBBLE  C o a r a a grained  2 - 16 ,5  Very coarse grained  ft  -.004  ,-7  Extremely fine  S-S C A L E FOR GRAIN OR PARTICLE SIZE. THE  PARTICLE DIAMETER  CH£MICAL  SIZE  SMALL  3.3  13  Pegmatltic  c I* -7S0Megapegmatitic  4m  MEDIUM PEBBLE LARGE  PEBBLE  SMALL  COBBLE  LARGE  COBBLE  SMALL  BOULDER  MEDIUM BOULDER  Cjttra-coarse megapegmatitic  2m  • nail 1 a p 1 1 1 i  PEBBLE  LARGE  BOULDER  large 1 a p i 11 i cobble-size b o a b s b blocks 362 724 1450  V. LARGE BOULDER  NOTE:l.It is q u i t e permissible to intermix the alphabetic w i t h t h e n u m e r i c symbols o f t h i s S - S c a l e , whenever w o r k d«3rands i t — no c o n f l i c t ensues by d o i n g s o .  e x t r a large bombs S blocks  (CF) and  40  4 I  42  FF CF »C MP UPPER T I E R F i n e Coarse Percent Maximum HEADINGS Fraction Fraction Coarse Particle (SCALE) ( S -Sea le) ( S - S c a l e ) (C-Scale) (S-Scale) ;; ; _ .: m m m * :—— — = — — 3 — a SH SR " R N " " L 0/C LOWER T I E R D e g r e e o f D e g r e e o f S h a p e o r O p e n / C l o s e d HEADINGS Sorting RoundedSpheric- Structure r.ess ity Equigranular (SCALE) (N-Scale I N - s c a l e IC , P , M , L , / I n e q u i g r a n . 1 CO 9) 1 to 9) P . B , E or" H-Scilel (0 , C , E .I )  /  ..  =  -105-  90 100  - I CoaraaPr ic i. ion  This «-scale, used f o r t h e Per Cent C F , is the G - Scale  symbols detail  3. For S e r i a t e T e x t u r e , i n w h i c h t h e G r a i n S i z e v a r i e s g r a d u a l l y c o n t i n u o u s l y , e n t e r s i g n i f i c a n t Fine P a r t i c l e size i n F F , u i F ( 3 9 ) / oivi t h e Large end o f t h e range i n MxP, i n F ( 4 2 ) /  J9  2.5 5  boulder-size bombs & blocks  2. Use t h e S - S c a l e f o r F i n e F r a c t i o n ( F F ) , Coarse F r a c t i o n Max P a r t i c l e kM P) i n F ( 3 9 , 4 0 , 4 4 2 ) /  COLUMN  .01 .OJ  or  GRAIN  GEOLOG"SYSTEM  l n l a r n a i l o n « l Q M « y t t * f n s Corporation  DECR£E  O f SOHTINC  1 S U  r i t i c M i y poorly iort«d v t r y p o o r l y t o r Ltd  poorly  s o r r.«d  nad#r*rtly  poorly  •Oder * t e l y  t o e ted  »->Jirt » t • 1 y we 11  well t o t l t d v«(y  we 11  ciutMly  torted  well  sorted  tor ted  DCGREE O r H O U M D H L S i 40L • i t c t M l y *n<jul*r  very ancjulAr •tnqular a o d e r t t e l y angular  iHAPtlalph-O  HI CITY 11-9)  OPEN ( 0 ) o r C L O S E D (C) bTKUCTURt or EUUI-IE) or iNtUUl-(1) I* KAN U LAW  inittHd i*t«  • t o d e r * L e l y rOundeu rounded vrry rounded e a t i e a w l y rounded  •QOO  6-op»n/i>.*r ted •ftw) o i i l y o l 1*1 y « r p*w t l d m  .ng  nut  U>ULII-  one «not(it:i  C"Cloe*o/ini.ci **> ) u i i t y o t per l i c i t * or  Po  toucti t 4 1 L t t - f t c e i e 1-9  For Open ex C l o s e d S t r u c t u r e t M a t r i x - s u p p o r t e d o r F r a r e w o r k - s u p p o r t e d ) , e n t e r 0 o r C i n F(42)L For Degree o f S o r t i n g <S«) and Degree o f toundneae (RM) , e n t e r 1 t o 9 i n F ( 3 9 , 4 0 ) L For Shape, e n t e r C , F , M , L , P , B OR E (see t r i a n g u l a r diagram) o r , f o r S p h e r i c i t y , i n F(41)L  1 to 9  SIZE  ir  CHARACTERISTICS  LC -COLOUR The GEOSYSTEM LC-Colour Code i s an abbreviated, 2-character version of the more detailed GEOSYSTEM Colour Code (LBHU)• LC i s f o r Lightness-Colour. Lightness L-Scale C28 Lower T i e r w white* (also i n C29) 9 palest a pale 7 light 6 l i g h t e r (m.light) " ) 5 medium (50% 4 darker (m.dark) 3 dark 2 very dark 1 darkest N black (Noir, Nil=0% lightness) (*White=100% " )  Colour Range C-Scale C29 Lower T i e r R Red U brown (Umber) 0 Orange T Tan (khaki) Y Yellow L Lime (Y-G) G Green Q aQua (B-P) B Blue V V i o l e t (B-P) P Purple M Mauve (P-R) W White (also i n C28) A grAy N black (Noir)  E X A M P L E S 9R 8R 7R 6R. 5R 4R 3R 2R 1R W W  9 N  N 1A  palest red=pale pink pale red = pink l i g h t red l i g h t e r red medium red darker red dark red very dark red darkest red white (dead white) white (dead white) off-white black (jet black) black ( j e t black) charcoal black  $, as a s u f f i x a f t e r any colour code, becomes - i s h , as in R$ = reddish. In any 2-colour-code combination, as i n GB, the f i r s t i s pronounced as though i t has an - i s h as s u f f i x GB = greenish blue. Examples — R$ U$ OS T$ Y$ G$ B$ P$ A$  reddish brownish orangish tannish yellowish greenish bluish purplish grayish  RO OR AR RA AB BA AG GA GY  reddish orange orangish red grayish red reddish gray grayish blue b l u i s h gray grayish green greenish gray greenish yellow  YL GB BG UG OU 7C 5C 3C  yellowish lime greenish blue bluish green brownish green orangish brown etc. etc. leucocratic mesocratic melanocratic (C for -Cratic)  LBHU-COLOUR Grayness S c a l e w white 9A p a l e s t gray 8A p a l e gray 7A l i g h t gray 6A l i g h t e r gray 5A medium gray 4A darker gray 3A dark gray 2A very dark gray 1A darkest gray N  black  In Geosystera C o l o u r , the three components of c o l o u r are L i g h t n e s s , B r i g h t n e s s and Hue. Think of t h e 24 hues as being equally spaced around the equator of t h e . c o l o u r sphere. The Lightness i s the v e r t i c a l component along the a x i s of the sphere, with white at the north p o l e , b l a c k at the south p o l e and medium gray at the componi n t e r s e c t i o n of the a x i s with the e q u a t o r i a l plane. The t h i r d ent, B r i g h t n e s s , i s the r a d i a l d i s t a n c e ' from and p e r p e n d i c u l a r to the a x i s : f u l l b r i g h t n e s s ( i e , b r i l l i a n t ) can only be a t t a i n e d at the e q u a t o r i a l s u r f a c e of the sphere.  (Noir) LBHU  L- S c a l e o f . LIGHTNESS  B- S c a l e o f BRIGHTNESS  W  white  9  palest -c  9  brilliant  8  pale(v.light)  3  v.bright  7  light -c  7  bright  6 '1ighter(m.1. )  6  brighter  5  medium - c  5  moderate  4  darker  4 . duller  3  dark - c  3  dull  2  v.dark - c  2  v.dull  1  darkest -c  1  grayish  N  black  A  gray  (m.d.)  (Noir)  HU, Range o f HUES R OR U RO 0 YO T OY Y GY L YG G BG Q GB B PB V BP P RP M PR R  E x a m p l e s  RED 96R orangish-red BROWN (Umber) 53U reddish-orange 790 ORANGE yellowish-orange TAN 7 T orangish-yellow YELLOW 87T greenish-yellow LIME yellowish-green 53YG GREEN bluish-green 34BG AQUA greenish-blue BLUE 22B purplish-blue VIOLET 3 BP bluish-purple PURPLE 65RP reddish-purple MAUVE purplish-red 1A RED ( r e p e a t e d ) 2A  (- c = any c o l o u r ) Lower t i e r :  Code  (any L v a l u e 1 - 9) L B H U ( w i t h any B-value) 28 29 30 31 (and p l u s any HU)  p a l e s t b r i g h t e r red (pink) medium d u l l brown light brilliant  l i g h t (moderate*) tan pale bright yellow  med. d u l l  yellowish-green  dark d u l l e r b l u i s h - g r e e n  v.dark v . d u l l b l u e  dark (moderate*) b l u i s h purple l i g h t e r moderate r e d d i s h purple d a r k e s t gray v.dark gray *  » any c o l o u r  orange  moderate presumed because B value l e f t blank  GEOLOG "SYSTEM  IM- SCALE  Iniai national Qaoairale>niGo<poiat ion  A SINGLE-DIGIT, NUMERICAL N-SCALE, f o r d e s c r i b i n g roundedness to  and s o r t i n g ,  ten,with I n most  5 always respects,  and i n t e n s i t y ,  i n the central,  degrees  e t c . ,in their  median  of l i g h t n e s s ,  natural  sequence  brightness,  from  d e g r e e of  1 t o 9 or f r o m  zero  that  dis-  -9  position. -8  t h e N-Scale  i s very  simple,  b u t i t has c e r t a i n  aspects  need  some  -7  cussion. The N - S c a l e preserve ven  located the  resent  0 t o 10, w i t h  form.  In this  t h e N-Scale  a t the centre  case,  This  equal,  points  described  mark  intervals  b y t h e Roman N u m e r a l  intervals  the divisions  as c o n s i s t i n g  is illustrated  unit  represented  i n F i g .A, t e n equal  the eleven  i s better  o f nine  t h e 10 b e i n g  As shown  a t t h e t o p and bottom.  zero  l i e between between  o f 9 equal  i n F i g . B, i n w h i c h  -6  X, t o  these  -5  ele-  the ten inter-  intervals  with  the digits  a  -4  half -1  1 to 9are  and t h e 0 and X a r e a t t h e o u t s i d e  -2  ends o f  full  which  nothing  intensity,  as  f o r instance,  Note  assigned N-Scale  i s blacker  values is that  than  that  and t h e r e f o r e  part  cannot  3 and 7 a r e always  a qualifier;  t h e 4 and 6 u s u a l l y  qualifier.  5 i s always  For instance,  i s j e t black  (N)j while  X can represent  represents  medium g r a y ,  of 0 - N » black black  t h e zero  exists  the scale  i n the T-Scale,  presence.  t h e N-Scale  o f the N-Scale,  the n i l intensity  in particular  5 then  t h e range  GEOSYSTEM S c a l e s ,  t h e X, c o m p l e t e  which  (W).  In contrast,  some a p p l i c a t i o n s  to  absence;  of lightness,  i s dead w h i t e  9.5 t o 10, b e c a u s e other  complete  absence  interval.  Unlike  -1  represents  complete  lightness,  For  from  two h a l f - i n t e r v a l s . The  a  0 t o X.  However,  interval  extends  the single-digit  points,  vals.  -X  be used  the middle,  whiter  requires  no a s s i g n e d  position  and/or  ranging  from  i n place  a fairly  (weak,  and part  values:  1 is It  strong;  as a q u a l i f i e r ;  intermediate,  soft,  from  In i t s a p p l i c a t i o n  does n o t .  Note  hard,  i n some o f t h e o t h e r  b u t in a l l these  also  etc.);  another  instances  characteristic  t h e 2 and 3 usually  and t h e 1 and 9 usually  moderate, e t c .  Fig.B is  2 i s 2 ; 3 i s 3i and so o n .  may b e b l a n k .  o f the G-Scale,  o f the N-Scale.  of X - W • white  white.  the X position  (X) i n t e n s i t y  -0  Fig.A  4.5 t o 5.5,  0 t o 0.5 a n d t h e r a n g e than  -0  complete  0 t o X o r 1 t o 9 o r 0 t o 9 , e t c . , a r e used  o f the S-Scale,  unqualified  have  and nothing  b u t the complete values  i s from  0 can rep-  have  scales,  they' have of the a very as  h a v e an ex t r e a t s l y as a  N•SCALE Some o f X 9 Ii 7 6 5 4 1 2 I 0  t h e more  comon  applications  of  che N - S c a l e  X  Alteration  9 7 6 S 4 3 2 1 0  Facies  cj inl l iocr ii :- /uto| tudjur st i c f l o o d i n g UQCiSSlC advanced j n j i l l ic phyllis/«jnaissenoui Kt" - s t a b l e int«*rra»jJi4ta jrqillic aontraorillonitic propyl u u fresh, prinary rock  4  3 2 1 0  Brightness X 9 b r i l l i a n t red or 8 very b r i g h t red 7 bright red 6 brighter red S moderate red 4 duller red 3 d u l l red 2 very d u l l red 1 d u l l e s t red 0  i n Porphyry  • Ju^njsuc, Abundant - ;or,.Tiwiily p r «j s «j n t ; o o d . • ur.cotnaori *> m i n o r • jriqinjt  in  the following  exceptionally h i g h amount o r i n t e n s i t y o f a l t e r a t i o n o r extremely high of mineralization very high or of fracturing or silicification high fairly high or i n d u r a t i o n moderate or s p h e r i c i t y , etc. f a i r l y low low v e r y low extremely low nil  9 8 7 6 5  extremely w e l l sorted o r graded or f o s s i l i z e d very well sorted or ripple-marked well sorted or re-worked, etc. fairly well sorted intermediately sorted f a i r l y poorly sorted poorly sorted very poorly sorted extremely poorly sorted unsorted  Lightness X » W = white p a l e s t red o r any c o l o u r 9 8 pale red (pink) 7 l i g h t red 6 l i g h t e r red 5 medium r e d 4 darker red 3 dark red 2 very dark red 1 darkest red 0 - N ' b l a c k IN f o r N o i r )  * * * J  are i l l u s t r a t e d  any  colour  Environment  A L T E R AT I 0 N M I N £ RA L S i b u n . QZ B I MS CLAY CL EP CB OTHER KA MM •  •  • •  • •  •  •  t  -* t  •  •  -  •  J  -  •  0 »  - -  i  •  MG , A H , T 0 , A K PP, T 0 , TE T 0 , F L , TE  •  t  • •  AB , ZE  Round ad n a a a / A n g u l a r i t y X 9 extremely rounded 8 very rounded 7 rounded 6 sub-rounded 5 intermediate 4 sub-angular 3 angular 2 very angular 1 extremely angular 0  GEO LOG'S YSTEM  MINERALS  l n l t r n « i i o M i G * o « y i l * m t Corpora I ion AC AD AB AM Al AX  AA AC All AN AP  AR AS AO  AU AT A: AE  BA BC BI B: BI a> BB< HB as BO Bit CA ca CT CE CM CC C> C. CP CL CD CR CK OL CS CN CY C: CY 0> <  MU  actinolice aJaUna albite d l m a n d i ce alunLce amphiDoles,gen andalus ice jnvj l e s i ce 68Pb annydrite anor c h l t e apatite d r a g o n l te. arsenopyrite 4 5As isoestos dug L t e ax i n i c e a i u c i c e I see M : ) 5dCu acgerine  ojrite uecy 1 Biotite b i o t i t e : hornDlende Tun.camb'n.undit* b i o c i c e alone B I >HB BI-HB BKHB hornblende alone  CZ CF CU CO CV CI  clinozoisics c o t f i n i ce copper,native cordierite covellite cupr ite  DC DC DI DO D:  dlckite d igen i te diopside dolomite dolomite : calcite min.comb'n.undif * dolomice alone DO>CA DO-CA DO<CA c a l c i c e alone  DO D> D" J< CA  Hi  hematite j magnetite min.comb'n, undi t* hematite alone HE)MG HE-MG HE<MG magnetite alone  HB HU HM HY  h o r n b l e n d e ( s e e B*) huebnerite 61W hydromica ( I L ) hypersthene  IL a n t e (HM) IM i l m e n i t e JO ] a d e i c e JA j a r o s i t e JO j o r d i s i t e  NF n e p h e l i n e NI n i c c o l i t e OL OP 00 OX OR  PH PF PT PO PS 3 2 T i PY PL PX PP 60Mo PR PN  EN ES EP ER  FO FA FT bismuth in i te 7 0 8 i FX bornite b )Cu FO orocnan t it e 5 bCu FR FM FL ca i c l t e ( s e e 0 : ) CL C : c a r b o n a t e s ,<jen c a s s i c e r i ce 79Sn 7 7PD GL cerussite c n a i c a n t h i ce 25Cu. C> chalcocice,gen accu • on e c . m m C< " on gangue SL chalcopyrIte 35Cu GA chlor ite chloricoid GS chromice 4 6Cr GN chrysocolla 36Cu CC chrysolite(olivine) CO chrysoc i l e CD cinnabar tJ6Hq CR clay CR clay ; muscovite GS m m . c o m b ' n , u n d i c• CY clay alone CY>.1U CY-.1U HA Cl<;MU IIV rauscovice alone HE HS  CX c l i n o p y r o x e n e , g e n  Cu HE H> 66Cu H« 8 9Cu I K MG  enarg1te enstdtite epidote e r y ch r i t e  KA KY KF K; 30Co KF K>  forster ite fayalite lamacinice celdspar9,gen feldspathoids,gen terberice w f errimolybdice 40MO 4 9F 11uor i te galena d6Pb galena : s p h a l e r i t e min.comb'n, undit" galena alone GL>SL CL'SL CL<SL s p h a l e r i t e alone garnet glass,gen glauconite glaucophane g o e t h i ce gold graphite greenockite gre isen,gen gypsum  K-  K< PF  LM LU LU LE LI HF MA MG MC M: MC M> M» M< AZ  kaolin kyanice K-spar,orchoc lase K-spar : p l a g i o c l a s e min.comb'n,undI£* K-spar alone KF>PF KF-PF KFCPF p l a g i o c l a s e alone  laumoncice lawson i te leuc i t e leucoxene 1imonlte ma f i c s , g e n magnesite 4BMgO m a g n e c i c e ( s e e n : ) 72Fe malachite StiCu malachice i a z u r i t e min.comb'n,und1£* malachice alone MOAZ MC-AZ MC<AZ a z u r i t e alone  02 OA QC OH QM QX OS QT QR OV  phlogopi te plagioclase(see K:) platinum Pt powellite 58Mo,W psilomelane Mn pyrite 47Fe pyrolusite pyroxene,gen pyrophyl1iCe pyrrhotite bOFe pentlandlte quartz,gen quartz,agate quartz-carbonate quartz,chert quartz,amethyst quartz,crystals q u a r t z - s e r i c ite quartz-tourma1ine quartz,rutilaced quartz vein,massive  RC r h o d o c h r o s l c e RN r h o d o n i t e RU r u c i l e SA SC SZ SF  SP ST SB 3u SX SR  talc tellurides,gen Te tennantiteS0CUS6Sb«As tenorite 80Cu tecrahednte CutSb TT,TN undIf topaz tourmaline cremolice  UR u r a n i n i t e ( p i t c h b l e n d e 9 2Ut UX u r a n i u m m i n e r a l s , g e n ~ VA v a n a d i n i t e VE v e s u v i a n i c e WD WO HP WN  7]Pb,llV  wad Mn • o t h e r wollasconite wolframite 62W wulfenite S6Pb*26Mo  ZE z e o l i c e s , g e n ZI z i r c o n ZO z o i s i t e  XX  YY 2Z XY  SH MS SE SD SI SV 68Mn SS SO SL  Au C MN m a n g a n i t e 78Cd MT m a r c a s i t e MR mar i p o s i ce ML m e l n i k o v i t e MI m i c a s , g e n MO m o l y b d e n i t e 60Mo MZ monaz i t e halice MM moncmot* 11 I o n i t e he l v i c e hematice,earchy 70Fe MU m u s c o v i t e ( s e e C : ) hemacice,specularite MS s e r i c i c e  TA 44.N1 TL TN TE oliv ine(chrysolice) TT opal TX opaques,geri TZ oxides,gen TO orthopyroxene,gen TR  Mn Mn X I 6 0 T i X2 Yl  any  mineral  •  •  •  •  ) minerals identl) t i e d elsewhere ) or later  sanidine scapolite A 0 D E N D UM : scorzalite sericite-fluorite assemolage scheelite 64W s e r i c i t e (MU) serpentine siderite 48Fe s i l l i m a n ite si lver silver & sulphosalts sodallte sphaler i t e (see G:) 67Zn spnene s caurol1te stionice 72SO sulphates,gen sulpnides,gen spe r r y 1 1 t e  MINERALS  GEOLOG'SYSTEM  InurnaltonalGMtyslanit Corporation  ro  RECAP SUMMARY OF SOME IMPORTANT G E N E R A L M I N E R A L S  RECAP SUMMARY OF MINERAL COMBINATIONS*  AX CB CC CX FX FD GL G$ LI MF 00 OX  Bi  biotite  C:  clay  amphiboles carbonates c h a l c o c i te c l inopyroxene feldspars £eldspathoids glass greisen 1imonite oafics opaques oxides  PF PX QZ SF SS SU SX TL TX UX ZE  assemblage  i  hornblende  : muscovite  Ds d o l o m i t e  i  i  calcite  G:  galena  Hi  hematite  i  Kt  K-spar  plagioclase  i  Mi m a l a c h i t e  sphalerite magnetite  i  azurite  i  N O T E S 1. R e : Use o f M i n e r a l Codes as Q u a l i f y i n g M i n e r a l ( Q a l m i n ) , Q M I fc Q M 2 , i n f i e l d F ( 3 2 - 3 4 ) / L on GEOFORM: E n t e r Code o f a n y m i n e r a l ( s u c h a s h o r n b l e n d e - H B ) f o l l o w e d by e s t i m a t e d p e r c e n t p r e s e n t i n t h a t i n t e r v a l , u s i n g G - S c a l e ( s u c h as * f o r .3% o r 2 f o r 2 0 1 , t h e r e b y c r e a t i n g t h e 3 - c h a r a c t e r Q a l o i n C o d e s , HB* a n d 1182. ( S e e GEOFORM H e a d e r ) 2.  R e : Use o f M i n e r a l C o d e s a s a n y m i n e r a l XX o r TY i n f i e l d s F ( 6 7 - 6 8 ) / L and F ( 7 5 - 7 6 ) / L i E n t e r Code o f o b s e r v e d m i n e r a l ( s u c h as CT» c a s s i t e r i t e ) i n Upper T i e r 6 7 - 6 8 o r 7 5 - 7 6 : How i t o c c u r s i n Lower T i e r 67 o r 7 5 ; and t h e e s t i m a t e d p e r c e n t amount i n Lower T i e r 68 o r 7 4 , r e s p e c t i v e l y (See GEOFORM H e a d e r b e l o w )  * m i n . c o m b ' n , u n d l f > m i n e r a l c o m b i n a t i o n , u n d i f f e r e n t i a t e d . F o r i n s t a n c e , u s e B: where p r o p o r t i o n o f BI 4 HB c a n n o t be g i v e n . N o t e t h a t many o f t h e m e t a l l i c m i n e r a l s have i o f t h e i d e n t i f i e d m e t a l shown a t r i g h t . Quartz,S\ i n veins; Epidote,.IX in blebs; Cassiterite..3t in m i c r o v e i n s ; Marcasite, It disseminated-  81.050  International Qeoayatame Corporation  Vanoouvar,  Canada  GEOLOG'SYBTEM  ROCKS  Inter national O M a y s t e m . C o r p o r a 11 o n  Tha f i r s t 4 l e t t a r a o f a r o c k t y p e na«e i a i t s p r e f e r r e d C o d a ( g r a n i t e - GRAN - GR and d i o r i t e - DIOR - DR) where GR i DR a r e t h e S h o r t F o r m a , u s e d f o r f o r m i n g compound r o c k names ( g r a n o d i o r i t e - GRCR, q u a r t z d i o r i t e • QZDR), b u t i f 4 t h l e t t e r i s a vowel (as i n a p l i t e ) , t h a t vowel i a r e p l a c e d by t h e next c o n s o n a n t ( a p l i t e « A P L T , a r g i l l i t e - ARGL, a n d a n d e s i t e • ANDS), a n d i f a d o u b l e l e t t e r o c c u r s w i t h i n t h e f i r s t 4 ( a s i n a g g l o m e r a t e ) o n * i a d r o p p e d ( t o become AGLM) CODE SHORT ROCK TYPE NAME FORM FORM acidic rock,gen ACID adamellite > ADAM AO QM q uartz monzonite (OZMZ) agglomerate AGLM AG AG " a l t ' v form AGXX AL alaskite ALAS alnoite ALNT AM amphibolite AMPH AM " a l t ' v form AMFB AN andesite ANDS " dyke AN/D " flow AN * F " sill AN 5 L anorthosite AN0R AP aplite APLT " dyke AP/D AR argillite ARGL AK arkose ARKS AC autoclastic rock AUTC I BENT BN/B BASL BS/D BS»F BASC BI3C BONE BRXX BRAC BRAF BRAI BRCQ BRQC BRVC BRVL BRCL  CARS. CRBN CHER CLIN CYSH CLAY 0/CY  BN  bentonite " bed basalt " dyke " flow b a s i c rock.gen(MAFC) BC b i o c l a s t i c rock,gen bone c o a l BR b r e c c i a , g e n autoclastic breccia " flow " intrusion " carbonate-quartz " quartz-carbonate " volcaniclastic " • volcanic " chlorite BS  CH  CS CY  carbonatite " alt'v form chert clinopyroxinite ( o r u s e PERD.CX) clayshale claystone clay unconsol.as in overburden  C0AL C0 C0AN CPSA C0BT C0SB C0LG (B0NE) C0NG CG CGXX CG CGEC CGEV CGIG CGVL CGVC C  j  3  Q  N  DACT DIAB DB/D DBSL DIAT DYKE DI0R OR/D DRSL DRIF D0LM D0RF D0/B DUNT  C  Q  DC DB  DI 0/ /D DR  D0  coal CABR " anthracite GNIS " s e m i - a n t h r a c i t e GNES bituminous GRAN " cub-bituminous GRTC * lignite GRNT " bone GRDR conglomerate GD/D " alt'v form GRFL " epiclastic GRBL " epivolcaniclast •GRLT " igneous GSCH " volcanic GSTN volcaniclastic GWAC coquina GWTF GRIT  GB CN GN GR GT GT GD  Gt GS CW  HARZ HBIT II0RN HRNF (BRHY)  dacite diabase " dyke " sill diatomite dyke(dike)rock " alt'v form diorite " dyke " sill drift, glacial dolomite " reef " bed dunite  IGNS IGNM INTR  ECLG EPIC EPVC  EC EV  EXTR  EX  eclogite epiclastic rock* epivolcaniclastic* (•see D e f i n i t i o n s ) e x t r u s i v e rock  FALT FELS FL0W  FL IF  fault(zone)or felsite flow rock  FAUL  gabbro gneiss " alt'v(regular) granite granitic rock alt'v form granodiorite " dyke granofels granoblastite granulite°granolite greenschist greenstone greywacke-graywacke " tuff grit  harzburgite(PERD.0L) hornblendite hornfels alt'v form h y p o c r y s t a l i n e brec  IG IN  igneous rock ignimbrite intrusive rock  JASP JSPD  jasper jasperoid  KIMB  kimberlite  LAHR LAMP LM/D LAPL LATR LATT LAUR LAVA LHER LIMS LS/B LSRF LSSQ L0ST  LM LP LT LV LS  1 ahar lamprophyre " dyke lapi l l i s tone later it e latite laurvikite lava lherIO1ite limestone " bed " reef " sequence lost core  MAFC MFIC MFVL (TRAP) MARB MARL MSXX MS0X MSSI MSSU MSSX MARK MTBC METM MTDB MTSD MTVL MTVC MIGM MILL MINT M0NZ MUDS MYLN MISS  MP MF TP  MX  MB MT MS  MZ MD  NELS NFS Y N0RD N0RT 0LGB 0RGN 0RPY 0VER 0/CY 0/GV 0/SN 0/SI 0/MD (S0IL) (TILL)  mafic rock,gen " alt'v form " volcanic mafic rock • t r a p marble marl or marlstone m a s s i v e a n y m i n XX " oxides " silicates " sulphates * sulphides meta-arkose metabioclastite metamorphic r o c k . g n . metadiabase metasediments,gen metavolcanics,gen metavoleaniclastics,gen migmat i t e mill-rock minette monzonite mudstone mylonite u n l o g g e d p a r t o f DH  nelsonite nepheline syenite nordmarkite norite  0/  o l i v i n e gabbro orthogneiss orthopyroxinite(PERD overburden" CX) clay, unconsol gravel " sand * silt mud " so i 1 t i l l , glacial  PAGN PEGH PERD PERT PHON PHY L PICR PPXX PPFX PPFO PPQF PPQZ PYRC (AGPC) (BRPC)  PG  PH PP  PC  PYRX  I  QZIT QZDR QZGB QZMZ QZPH QZ/V QZVN  paragneiss SCHI pegmatite SCHS peridotite SCYL perthosite SEAT phonolite SEDM phyllite SERP picrite SAND porphyry ,gen 10/SN) " .feldspar " , f e l d s p a r - q u a r t z SILT " . q u a r t z - f e l d s p a r (0/SI) SHAL " .quartz SNSI pyroclastic rock SNSH agglomerate SNCG " breccia SHSI SISN SISH SICG pyroxenite  QD QG QM QP  RHYL RY RHYD RD ROCK RX RX-1 RX-2 (EC-1) (EV-11 (MS-1) (VL-1) (VC-1)  quartzite quartz diorite quartz gabbro quartz monzonite quartz phyllite quartz vein(s) alt'v form  rhyolite rhyodacite rock,gen rock-1 ' rock-2 • epiclastic-rock-1 * epivolcaniclas.-1 * metased.-rock-1 * volcanic-rock-1 * volcaniclas-rock-l« (•identified laterl  MOTS THAT  SLAT SOIL SYEN SYDR TACT TILL TLIT TING TONL TRAC TCAN TRAP TR JN TUFF TFAQ TFLP TF XT TFXL TFWL TUFS  SI SI  SN SI SH  SL SY  TC  TF  schist alt'v form scyelite seatearth sedimentary rock serpentinite sandstone sand u n c o n s o l siltstone silt unconsol shale sandstone w i t h SI with shale " w i t h conglom " with siltstone s i l t s t o n e w i t h SN " with shale " w i t h conglom (•interbedded,50t-) slate soil (overburden) syenite syenodiorite  ULMF ULBS  UM UB  ultramafic ultrabasic  V0LC VLCC VEIN  VL VC /V  < < < < . > > >  < < > >  volcanic rock volcaniclastic vein microveins macrovein websterite wehrlite  WEBS WEHR  rock .alt'v  rock  tactite t i l l , glacial t i l l i t e tinguaite tonolite trachyte trachyandesite trap tronghjemite tuff " .aquagene  " .lapilli "  .crystal .crystal " .welded tuffasite  lapilli  1) The above table i s alphabetic by rock type names, not by their Codes 2) Somm rock types have more Chan one Code: the second i s an alternative form; both are acceptable System and both may be used the same project and sane log, as for instance to two different rock units hav i ng the same rock type )) Codes in brackets are the Codes of rock types not in their alphabetic position  in  by the  distinguish between  ROCK-TYPE  QUALIFIERS  In a d d i t i o n t o T y p i f y i n g and Q u a l i f y i n g M i n e r a l s , two o t h e r f a c t o r s o f i m p o r t a n c e qualify a rock n a m e l y . E n v i r o n m e n t o f E m p l a c e m e n t and R o c k - T y p e Q u a l i f i e r , b o t h o f w h i c h a r e 2 - l e t t e r c o d e s t h a t a r e t o be e n t e r e d s i d e - b y - s i d e i n t h e Lower T i e r , d i r e c t l y below Rock T y p e . A l t e r n a t i v e l y , R o c k - B o d y Form a n d / o r P r o v e n a n c e may be e n t e r e d i n t h e s e same two f i e l d s . . ENV ~ AC AL AO AT BH BK BR BS CO EC EV FL FR GF GL IN LC LG MR MS MM MD NM PC PL SD SV VL VC  ENVIRONMENT OF EMPLACEMENT  RTQ —  ROCK-TYPE  autoclastic allochthonous  AN AP  andesitic aplitic  aeolian autochthonous  AR AX  biohermal brackish-water  BN CH CY CO CG DC DB DR DO FL GB GR GN HR LT LS MF MZ  argillaceous arkosic bentonitic cherty clayey coaly  back-reef biostromal continental epiclastic (non-volcanic) epivolcaniclastic fluvial, fluviotile fore-reef glacio-fluvial glacial, glacio-lacustrine intrusive lacustrine lagoonal m a r i n e , gen marine, shallow marine, moderate depth marine, deep water non-marine pyroclastic plutonic sedimentary sub-volcanic v o l c a n i c , gen volcaniclastic  PG PH PP RY RD Sit SH SI  QUALIFIER  conglomeratic dacitic diabasic dioritic dolomitic felsitic gabbro i c granitic gneissic hornfelsic latitic limey mafic monzonitic pegmatitic phyllitic porphyritic rhyolitic rhyodacitic schisty, shaly silty  -ose  SL SY TF UM VL  slaty syenitic tuffaceous ultramafic volcanic  RBF B/  c/ D/ F/ F= N/ P/  s/ S= S#  $/ V/  - - ROCK-BODY FORM bed contact  zone  dyke f a u l t zone flow v o l c a n i c neck pipe seam sill stock stringer vein  zone  PRV  —  PROVENANCE o r  SOURCE OF ROCK M*  metamorphic  X* P*  mixed plutonic  Y* S*  pyroclastic sedimentary  V*  PARTICLES  volcanic  (*The a s t e r i s k may be r e p l a c e d w i t h a G-Scale percentage M3 = 3 0 % m e t a m o r p h i c P4 = 4 0 % p l u t o n i c S6 = 6 0 % s e d i m e n t a r y )  STRUCTURE GEOLOG*SYSTEM lnl«intiion«iQ*o«|r<lwntCoipoi<lion STRUC 1 i U p p e r •T, T i e r MODE F e a t u r e THKI 0 / HESS B  Lower Tier L  Bx -T 2  48  STRUC 2 Feature I •  49  SO  T  STRIKE >90*l D I P AZIMUTH < to right clockwise tf * o r f r o a T r u e Tops[ PLUNGE North downi(linear) T ! 0 I P or o r AZIMUTH a i PLUNGE 51  52  53  54  | SS  - s c A r. •  M O D E  T H I C K N E S S  Assgn Scale Value Value < 2 mo  1 mm  0  varved  < 5 mm  3 mn  1  laminated  .5 t o  <  2cm  1 cm  2  very  2 to  <  5cm  3 cm  3  t h i n  5 to  <20cm  10 cm  4  aed.  20 t o  <50cn  30 cm  5  m e d i u m  .5 t o  < 2 m  1  a  6  med.  2 to  < 5 m  3  m  7  t h i c k  5 to  < 20 m  10  a  8  very  >20 a  30  a  9  extrmly thk )  2 to  56  The a z i m u t h o f a s t r i k e i s m e a s u r e d c l o c k w i s e from T r u e N o r t h and i s e x p r e s s e d a s a 3 - d i g i t number, e v e n i f l e s s t h a n 1 0 0 * , a s f o r i n s t a n c e , 037 a n d 175, t o d i s t i n g u i s h from d i p s , which a r e 2 - d i g i t . An a z i m u t h t h a t i s due n o r t h i s b e t t e r e x p r e s s e d a s 360 r a t h e r t h a n 0 0 0 .  B e d d i n g Splitting o r Description Textural Tern  The s t r i k e o f a d i p p i n g p l a n a r f e a t u r e t h a t i s n o t v e r t i c a l c o u l d be g i v e n a s e i t h e r o f two v a l u e s w h i c h would d i f f e r by 180*i h o w e v e r , i n GEOLOG, u s e t h e c o n v e n t i o n of f a c i n g along that d i r e c t i o n of s t r i k e that p l a c e s the d i r e c t i o n of d i p to observer's right.  ) ) fissile ) flaggy  11  slabby  SB  ) ) ) blocky  BK  thin  thin  thick  thick  PS  % 1  ) ) \ ) J massive 1 }  MX  If t o p s a r e down, s t i l l take s t r i k e so that d i p i s to r i g h t , b u t r e c o r d d i p as a n g l e g r e a t e r than 90*. If planar feature is vertical, face s t r i k e direction t h a t p l a c e s t h e presumed t o p o r y o u n g e s t s u r f a c e t o t h e right. If taking a t t i t u d e of planar feature having thickness, s u c h a s d y k e , d i s t i n g u i s h a t t i t u d e o f t o p w i t h T i n 54 f r o m a t t i t u d e o f b o t t o m w i t h B. However, n o r m a l l y r e c o r d a t t i t u d e o f t o p o f dyke when F r o m - f o o t a g e marks inters e c t i o n w i t h t o p and r e c o r d a t t i t u d e o f b o t t o m s u r f a c e when F r o m - f o o t a g e marks b o t t o m .  The  B  can  also  mode  x  and B  2  be u s e d  thickness  seams, feature  i n F(48)/L,  veins,  of  f o r t h e more  general  litho-features,  e t c . , which  I D fields,  f o r bedding  must  F(49-50)/L.  such  mode  thickness,  Ti_ a n d T j , f o r as dykes,  be i d e n t i f i e d  coal  i n the  F  AX  E  A  T  U  R  E  I  D  BN BD  a x i s of. a n y f o l d - may r e p l a c e x w i t h : A anticline S syncline 0 drag f o l d , etc. banding b e d d i n g ; B I , B2 . . s p e c i f i c  CV C/  cleavage; contact ;  IC, CI,  U/  dyke; - may  02 . DT •  F/ FB FZ FS  f a u l t ; F l , F2 flow banding f a u l t zone fracture set  GN  gneissosity  JS  joint  LS LN  lens ln.eation;  S/ Sit $/ SS  s e a m ; S I , S2 . shear stringer slickensides  U/  unconformity;  V/ << >> VC VQ  v e i n ; V I , V2 . microveins macrovein vein, calcite vein, quartz etc.  01, use  2C . C2 .  . .  E  N  T  beds  .  specific  .  .  (alt.form, bottom  DK)  (alt.form,  FL)  faults  •  single  .  fracture)  single  specific  joint)  lineations  specific  UA a n g u l a r .  S  CN)  (Sj~-  .  E  B/)  ' (SF  L2  I  (alt.form,  set  LI,  T  specific cleavages ' • contacts (alt.form,  . s p e c i f i c dykes d y k e t o p , OB • d y k e .  I  seams  unconformity  specific  veins  TEXTURES 00  o  o  AM A* Afi AP AG  a l g a l matted amygdaloidal animal bored,burrowed aplitic augen s t r u c t u r e d  BN BD BC BI  banded bedded bioclastic bioturbaceous=dist u r b e d by a n i m a l s blocky botryoidal brecciated  BK BT BR  I  (C (X (F (L CA CM CT CS CG CC KR CR XB XC DF  EQ  casted crystal-casted flute-casted load-casted cataclastic c h i l l e d margin clastic closed-structured framework s u p p o r t e d clay-galled concretionary crackled crenulated cross-bedded cross-cutting drag-folded* en ech. s h e a r i n g equigranular  FZ F$ FY FL FT FB F2 F3 F5 F7 F9 FO FS F( FC FF FG FM FN FP  f e l d s p a r zoned fissile flaggy flaser-structured flattened flow banded folded s l i g h t l y " lightly " moderately " strongly " tightly foliated fossiliferous "-calcareous "-carbonaceous "-faunal "-graphitic "-marine "-non-marine "-plants  GP GN Gj GT GB GL GF GY  glomero-porphyritic gneissic graded-bedded granitic granoblastic granulosa graphic greasy, s e c t i l e  HT HO HF  IM IQ IB IN  imbricated inequigranular interbedded interstitial  LM LB LN LE LS LL LT  laminated lensoid-banded (streaky) lenticular lineated listric-surfaced lit-par-lit lithic  >> MX << MC MY  macroveined massive microveined mud-cracked mylonitic  ND  nodular  OS  open-structured - d i s r u p t e d , matrixsupported  PW  p a r t i n g s & whisps of c o a l pegmatitic peletoidal penecontemp.slumped  heterogeneous PG homogeneous PL h o r n f e l s i c s t r u c t u r e d PS  PH PI PK PP PB TG RP RW R7 R5 R3 R2 RB RM M7 M5 M3 RA RS SC SR SB SL SS SP SK SW ST TC TG UF W VS VG WL  phyllitic p i s o l i t i c , pea-like poikilitic porphyritic porphyroblastic ptigmatic rain-printed reworked s t r o n g l y RW m o d e r a t e l y RW l i g h t l y RW s l i g h t l y RW r i b b o n - l i k e , -banded ripple-marked s t r o n g l y RM m o d e r a t e l y RM l i g h t l y RM ( e t c . ) asymmet. RM symmet. RM schistose scoured slabby slaty s o f t sediment slumping sparry stockworked stromatolitic stylolitic trachytic, trachytoid ptigmatic uniform t e x t u r e d veined vesicular vuggy welded  TYPIFYING & QUALIFYING T Y P I F Y I N G MINERALS AND QUALIFYING MINERALS,  ROCK-  Forming Minerals  2-Code  for  Typifying Minerals  actinolite albite  AC Afl  andalusite  BI  calcite  8 I  CA  clay c 1inozois ito  3-Code Q u a l i f y i n g , Materials, Minera l s fc D e s c r i p t o r s ACt Aflt AMG AMt AAt ARG ARK  epidote  feldspar,gen  garnet glaucophane graphite  CA GC GR  tiat HY%  hematitic hornbleodic hypersthenic  j a d e i te K-apar kyanite laumonite lawsonite  JDt KF% KYt LM% LWI  jadeite » K-feldspathic . kyanitic laumonitic lawsonitic  CYI CZI  clayey clinozoisitic  CCR CPU  coalyb co.rash " p a r t i n g s and whiaps * p e r cent cobbly pyrite conglomeratic  Micas,gen.  MI MM MU MS  MIt MRt MMt MUt MSt MTt MUD  limonitic limey lapilli t l i t h i c t (RXt) leached, n-1-9 N-Scale micaceous miarolitic montmor11Ionic muscovitic sericitic matrix t muddy  nepheline  NP  NFt  nephelinltic  olivine  OL  OL* OQZ  olivine t orthoquartztic  PR  PAR PEB PHS PY» PYN PYT PPt PXt PR*  partings pebbly phosphatic pyritlc pyritic-nodular pyritic-tubea pyrophy11itic pyroxinltic pyrrhotitic  QZ OA QC QV  QZ* OA* QCt QVt  quartzltlc.osa agatized cherty t m a s s . QZ-Vtl  rutile  RU  RXt RTL RUt  t rock frags rootlets rutilitlc  sericite  MS  MSt  sericitic  serpentine aider ite s i l Lii.iinlte  SE SO SI  SE* SD* Sit  serpentinizad sideritic silliminitic  t cordieritlc* pyrophylllte coquinoid pyroxene % coquina py r r h o t i t e t crystals  EPt . EVP EV%  quartz,gen dolomitized,ic - a>jate - chert epidotized - vein,mass. evaporitlc " p e r cent  FX I FLD FE*  feldspathic feldapathoidal ferruginous  G At GC% GR* CRT GY*  garnetiferoua glaucophanoua graphitic gritty gypsifarous  DOt  Lit LIM LPt LTt LCn  limonite  i.uDntmor 11 I o n i t e calcareous muscovite calcitic " sericite I carbonates carbonaceous t cherty t  XT* DO  HE*  CAL CAt CB* CR» Clit  cat dolomite  hemat i t e hornblende hyperathene  BR%  C0» COQ  MATERIALS a DESCRIPTORS  N 0 T E i T h e t h i r d c h a r a c t e r , t , p r e s e n t i n many o f t h e 3 - c h a r a c t e r c o d e s , i a t o be e i t h e r r e p l a c e d w i t h a G - S c a l e p e r c e n t a g e estimate o f t h e amount o f t h e m i n e r a l o r m a t e r i a l p r e s e n t , . . . o r l e f t b l a n k  bentonitic bioclastic biotitic bituminous 1 bleached, n1-9, N - S c a l e breccia t  BEN BIO BII BIT BL  CO I COB CGI cordierite  actinolitlc albitized aiuygdaloidal " , t amyg's andalusic argillaceous arkosic  MINERALS  PY PP  SAN SN* SIL SLt SIF  ST  topaz tourmaline tremolite  T2 TO TR  ZE ZO  zeolite zoisite  "  *  SLT S-E ST*  silty silty siliclfied -siliceous -n»needle hardness slatey seat-earth staurolitlc  TZt TOt TRt TKt  topaz t tourraallnlzed treraolitic tuffaceous  vst  vesicular  SFn  staurolite  sandy  XNt  xenollthic  ZE* zot  zeolltic zoisitic  1  * c o r d i e r i t e a n d c o a l h a v e t h e same 2 - l e t t e r c o d e - CO , b u t b o t h a r e n o t l i k e l y to o c c u r t o g e t h e r COAL MATERIALS PET LIG SBT BIT BTH BTM VTL SMA Kbit  SUMMARY  peat, peaty lignite,-ic sub-bituminous bituminous ", h i g h v o l a t i l e med. v o l a t i l e " , low v o l a t i l e semi-anthracite anthracite  RECAP SUMMARY Clayey to Cobbly CYt MUD SHt SIL SN* PEB COB  clayey muddy shaly silty sandy pebbly cobbly  APPENDIX C A N A L Y T I C A L RESULT  -121-  DOH 021 II 39109 6 8 . 08 39110 67 . 78 39112 67 . 53 391 14 67 . 64 391 16 6 6 . 89 391 18 67 . 61 39120 68 . 10 39122 6 7 . 75 39124 67 . 35 39125 62 . 1 1 39152 67 . 34 39154 67 . 78 39156 67 . 66  3. 14 1 .48 3. 45 1 .58 3. 27 1 .62 3. 42 1 .64 2. 83 1 .44 2. 86 1 .49. 3. 26 1 .52 3 1 1 1 .63 3. 38 1 .82 8. 68 6 . 13 3. 84 1 .87 3 14 1 90 3. 54 1 87  3. 50 3. 35 3. 45 3. 25 5. 86 3. 19 2. 60 2. 88 3. 35 2. 58 3. 38 3. 27 3. 03  3. 47 3. 62 3. 90 4 .09 1 .80 3. 96 4 . 16 4 27 3 93 1 .07 3. 94 4 . 22 4 . 15  3. 13 3. 12 3. 03 2 .86 5. 12 3 73 2 99 2 92 3. 07 2. 31 2 .84 2 89 2 94  0. 50 0. 14 0. 52 0 . 15 0 . 52 0. 15 0. 54 0. 14 0 . 45 0. 17 0 . 54 0. IS 0 . 47 0 . 14 0 . 49 0 . 14 0 . 51 0 . 14 1 .02 0 . 22 0. 54 .0- 15 0. 47 0. 14 0 50 0. 14  8 . 36 9 . 99 9 .65 6 .94 8 .79  4. 71 5 .21 6 .52 3 .52 5 .74  2 67 3 .67 2 .91 3 96 3 .71  O 34 0 .37 0 .69 0 .07 0 .85  3 76 3 .85 2 .80 4 .57 3 .47  0 93 0. 12 1 . 17 . 0 19 1 . 16 0 .20 0 92 0 .20 1 .02 0 : 15  1 1 50 . 10. 23 10. 32 13 07 7 .27 10 45 12 .72 10 .96 7 .47 11 .90  5 .68 6 . 64 6 . 92 7 49 4 . 19 6 .89 8 .74 6 83 6 .00 7 .40  1 .45 3. 10 3. 05 3 43 1 12 2 .80 2 .98 3 .23 3 .46 2 .76  0 20 0 13 0 . 14 0 . 43 0 39 0 37 0 .54 0 .51 0 .23 0 .66  3 58 3. 3 1 3. 31 2 84 2 43 3 35 3 . 34 2 94 3 .41 2 .86  1 .19 1 .12 1 .1 1 1 .09 0. 79 1 08 1 . 33 1 .09 0 .97 1. 1 1  0. 33 0 . 19 0. 18 0. 22 0. 15 0 17 0. 16 0 16 0 . 19 0 . 18  16 .58 8 .20 15 . 45 10 .OO 16 .45 1 1 .35 15 31 9 .77 15 . 18 10 .42 15 . 30 9 .36  5 .35 8 .66 6 .37 7 .95 7 .53 6 .27  4 . 44 4 .64 4 . 45 2 .97 3 81 4 .32  0 .67 1 . 13 0 .25 0 .69 1 21 1 81  4 OO 2 . 14 3 .55 2 . 34 2 . 15 1 .63  0 .85 1 .07 0 88 1. 1 1 1 . 13 1 . 10  0, 0. 0 0 0 0  15 20 21 33 20 18  16 .32 14 .59 13 .99 14 .64 15 58 14 .34 14 . 26 14 .38 15 .20 15 .79 16 .74 16 .68  1 .51 1 .27 2 .32 2 .82 2 .72 1 ,94 1 .25 1 83 1 .74 1 .63 1 .78 1. 1 1  4 . 14 0 .20 0 .30 0 .82 1 . 17 0 .61 0 .35 0 .42 2 .85 4 . 17 4 .73 5 .79  1 . 17 1 .95 1 . 14 0 .86 1 . 72 3 . 34 1 .97 2 .37 1 .09 1 .50 2 .09 1 .73  6 .93 6 .50 4 .86 5 . 26 5 -65 5 . 19 5 .25 6 .23 6 .90 6 .57 5 .67 6 .26  0 . 38 0 .36 1 .46 0 .47 0 .48 0 .47 0 .37 0 .45 0 .39 0 .40 0 .43 0 .39  0 0 0 0 0 0 0 0 0 0 0 0  . 18 . 12 . 13 , 10 . 16 . 16 . 13 . 18 . 14 . 16 .20 .27  14 14 14 14 14 14 14 14 14 14 14 14 14  . 96 . 95 .96 .96 . 82 .96 .97 .97 .96 . 92 93 . 94 . 94  DDH 025 -38150 63 . 42 14 91 39176 58 99 17 . 28 39178 60 08 15 99 39180 62 .90 17 .42 39182 59 98 16 . 7 1 DDH 026 39130 6 0 . 34 14 .94 39 132 60 38 14 . 79 39134 6 0 . 22 14 . 75 39136 5 6 . 87 14 . 74 39 138 67 37 14 95 39140 60 65 14 60 39142 55 34 14 77 39144 59 20 14 .83 39146 63 1 1 14 .80 39 148 57 .97 14 .84 DDH 068 39 194 60 39 196 56 39198 56 39200 59 39202 58 39204 59  .07 . 75 .87 .29 . 13 .71  DDH 069 39206 66 .64 39208 71 .55 39210 71 .42 39212 70 .00 39214 68 .26 39216 69 .76 39218 72 • 16 39220 69 .78 39222 68 .62 39224 65 .03 39226 65 .71 39228 65 .60  2 .26 1 .56 2 .24 3 .36 3 .28 2 .32 2 . 15 2 .55 1 .81 4 . 18 2 .52 1 .99  DDH 076 37252 68 37255 68 37256 67 37258 68 37260 69 37262 68 37264 65 37266 65 37268 65 37270 66 37272 67 37274 68 37276 70 37278 66 37280 65 37282 66  .54 .86 .07 .20 .03 . 16 .96 .64 .84 .05 .70 .84 .32 .28 . 12 .55  14 .96 14 .96 14 .97 14 .96 14 .96 14 .95 14 .97 14 .97 14 .95 14 .97 14 96 14 .95 14 .86 14 .96 14 .97 14 .96  2 .94 3 .58 3 85 3 .97 3 .87 4 01 3 .94 3 .36 4 .87 4 .73 3 .83 2 . 75 2 . 14 3 .40 3 .90 3 .27  2 . 13 2 .52 2 .47 2 . 76 2 .07 2 .43 3 .04 2 .45 2 .61 2 . 18 2 .21 1 .59 1 .97 2 .58 2 . 27 2 .25  3 .21 1 .76 2 .84 1 .80 1 .93 2 .21 3 .47 3 .82 3 .05 3 . 14 2 . 23 2 .84 2 .68 3 . 18 4 .35 3 .68  1 .68 2 .07 3 .04 2 .27 1 .80 1 88 2 85 2 .63 3 .41 3. 1 1 2 .77 3 . 16 2 .59 4 . 18 2 .99 3 .02  4 .09 3 .85 3 .32 3 .70 3 .94 4 .24 3 .37 4 .77 3 .20 3 .57 4 . 13 3 .83 3 .89 3 .30 4. 1 1 4 .03  0 .48 0 .50 0 .56 0 .51 0 .44 0 .47 0 .58 0 .44 0 .55 0 .51 0 .46 0 .39 0 .32 0 .53 0 .47 0 .47  DDH 078 37226 67 37228 68 37230 68 37232 67 37234 66 37236 66 37238 59 37239 67 37242 65 37244 68 37246 68 37247 65 37250 67 37201 65 37202 65 37203 67 37204 67 37205 66 37207 66 3720B 66 37209 66 37210 66 3721 1 67 37213 66 37214 57 37215 67 37216 66 37219 66  1) .41 .80 .30 .09 .65 .27 .32 .65 .90 .00 .03 .68 .25 .83 .85 .25 .59 .95 .79 . 77 .79 .88 . 17 .99 .86 .95 .71 .96  14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14 14  97 97 97 96 97 95 89 96 27 96 97 92 92 97 96 96 97 96 97 97 . 96 96 . 97 96 94 97 96 97 14 97 14. 96  3 .53 3 27 2 .88 4 .25 3 .46 3 50 7 .81 4 .35 4 16 3 16 3 1 1 3 82 3 64 4. 37 4. 68 4 .08 3. 72 3 89 3. 38 3..46 3. 78 3. 29 3. 05 3 23 7. 37 3. 14 3 19 2. 98 3. 40 2. 84  2 .53 1 .92 2 . 12 1 .65 1 .53 2 06 3 .67 1 .65 2 .53 2 00 1 83 1 .87 2. 0 3 . 2 .47 . 3. 57 2 . 72 2. 68 2 35 2 .08 2 06 2 12 2 25 2. 13 2 . 15 4 .67 1 .61 99 1 .77 2 . 48 2. 0 0  1 .43 0 .97 1 .45 3 . 33 3 .95 3 .41 7 .53 2 .60 6 .23 2 . 16 2 .69 5 .26 4 .39 3 . 15 1 89 1 78 1 .67 2 29 3. 05 3. 02 2 .87 2. 89 2. 77 2..76 7. 04 3..39 3 .09 3 66 2 .94 3. 06  3 .69 3 .67 3 . 78 2 .61 3 .43 2 .98 3 .07 2 OS 0 .68 3 .53 2 .75 1 .59 0 .62 2 25 3. 04 3. 32 1 .98 3. 60 3. 39 3. 84 4 . 24 4 ..28 4 .03 4 54 2..90 2 85 4 .34 3 .25 3 84 3 55  4 .02 3 .93 4 .07 3 .82 3 .64 4 68 2 .26 4 .46 6 .33 3 .91 4 OB 5 14 5..25 4 42 3. 70 3. 64 4 . 94 3. 87 4. 01 3 57 3. 26 3 .40 3 .67 3 44 3 54 3..55 3 .63 4 01 3 .60 3 97  0 0 0. 0. 0. 0. 0. 0. 0. 0 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0.  51 48 52 50 SI 53 99 48 45 50 45 42 48 60 68 56 49 52 45 48 49 49 49 46 87 39 50 48 54 47  o. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0.  17 16 19 18 20 20 22 18 21 16 19 19 20 22 23 19 18 20 20 19 18 19 18 19 21 16 17 18 20 18  14 . 74 14 . 96 14 . 89 14 . 96 14. 97 14. 84 14. 48 14. 93 14. 91 14. 97  4 . 23 2. 59 2. 88 2 34 i 84 1 .87 2. 12 2. 65 3. 55 2. 72  3. 79 i o . 58 2. 86 4. 20 2. 47 S. 31 2 . 27 4 . 72 0 . 95 2. 27 1 .70 3. 85 1 .90 6. 05 1 81 5. 64 2 . 20 5. 43 1 .40 1 .12  0. 0. 0. 0. 2. 0. 0. 0. 0. 2.  5. 56 4 . 30 4. 47 4 .63 4 . 90 4 .03 3. 74 4 . 98 5. 17 4. 54  0. 48 0. 36 0. 35 0. 37 0. 0 4 43 0. 40 0. 37 0. 38 0. 48  0. 0. 0. 0. 0. 0. 0. o 0. 0.  19 15 17 17 17 16 17 17 17 16  37222 66 .49 37224 67 .41 DDH 080 37314 60 .98 37316 68 .76 37318 68 . 37 37320 67 94 37322 6 9 . 5 4 37324 7 1 . 2 1 37326 7 1 . 0 8 37328 6 7 . 2 3 37330 6 6 . 9 1 37332 6 9 . 9 7  t.  06 07 09 85 95 83 1 1 95 20 72  i  0 . 16 0 . 16 0 . 18 0 . 19 0 . 17 0 . 17 0 . 22 0 . 19 0 . 21 0 . 19 0 . 16 0 . 15 0 . 15 0 . 21 O. 19 0 . 18  SAMPL  DDH  MO  PROJ  CU  ZN  NI  CO  PB  CO  AG  F  mn  SAMPL  ODH  021  PROJ  MO  CU  ZN  PB  NI  CD  0146  6  1520  231  18  3 .3  28  12  0 .52  500  440  39190  0146  3  7 10  96  35  1 .2  39  0 1 4 6  6  181  36  13  0 . 2  17  15  0 .33  360  4 10  39191  0 1 4 6  3  219  60  23  0. 4  420  470  3 9 1 1 0  0146  4  44  24  0 .3  15  13  0 .27  39192  0 1 4 6  3  391 1 1  0 1 4 6  4  4 1  156  66  2 .0  16  12  0 .75  500  415  39193  0 1 4 6  4  391  12  0 1 4 6  4  1 17  45  13  0 .4  15  14  0 .25  380  415  39194  0146  391  13  0146  4  96  25  1 1  0 .2  12  1 1 0 .32  380  340  39195  0146  3  480  39196 39197  59  0146  4  74  36  19  0  3  16  13  0 .24  380  0 1 4 6  4  80  91  36  0  8  19  16  0 .58  440  126  39151  0146  3  326  36  1 1  0  3  13  12  0 .90  380  349  39152  0 1 4 6  4  101  283  12  2 .8  18  13  1.77  420  386  3 9 1 5 3  0146  3  306  92  9  0 . 7  16  12  1 . 10  440  324  15  12  3 .86  105  430  391  14  391  15  39154  0146  4  234  378  12  3  6  39  0146  4  339  212  10  1  9  15  12  1 .65  440  357  0 1 4 6  4  35  34  8  0 .4  17  14  0 .25  420  360  155  39156  DDH  -  0 2 5  3 9 1 5 0  0146  69  2290  185  18  1  4  19  29  2 .57  720  345  39176  0146  170  2720  224  19  1 . 7  22  47  2 .67  640  440  39177  0 1 4 6  140  2010  1 12  8  6  21  39  1 .78  700  460  39178  0 1 4 6  51  2560  88  1 1  0 .5  19  36  2 .89  740  470  3 9 1 7 9  0 1 4 6  380  1850  90  7  0 .8  19  32  1 . 77  840  320  3 9 1 8 0  0 1 4 6  96  2730  183  33  2 .0  18  32  1 .79  880  610  39181  0 1 4 6  140  3120  127  17  1 .0  19  32  2 .60  1040  39182  0 1 4 6  42  3050  80  12  0  8  19  49  2 . 17  840  3 9 1 8 3  0 1 4 6  2 6 0  3950  53  3  0  4  17  4 1  2 .95  1500  39184  0 1 4 6  100  3850  38  3  0  4  17  31  1 . 9 1 1 120  3 9 1 8 5  0 1 4 6  210  26G0  155  39186  0 1 4 6  25  2630  6 2 0  14  39187  0 1 4 6  310  1740  990  84  3 9 1 8 8  0146  230  2740  62  10  3 9 1 8 9  0 1 4 6  160  2090  770  29  DDH  .  37  0  38 4 20 34 19  7  22  30  2 . 13  920  323  5 .5  20  30  2 .76  780  610  7  13  13  4 . 13  800  7 20  1 . 3  12  1 1  1 .65  1200  29  7  16  17  2 .40  1 120  47  1 13  2  0 2 6  3 9 1 3 0  0 1 4 6  6  830  106  13  0  3  15  26  2  13  480  460  39131  0 1 4 6  17  500  B4  26  1 .2  15  24  1 .. 3 3  600  275  39132  0 1 4 6  13  630  115  45  1 .2  16  26  10  680  365  3 9 1 3 3  0 1 4 6  13  680  62  10  0. 7  1 1  19  1 .3 4  700  171  39  0 1 4 6  40  510  56  9  0. 4  16  42  1 .9 8  600  303  3 9 1 3 5  0 1 4 6  5  3010  61  14  0. 4  17  34  8  440  304  3 9 1 3 6  0146  24  2060  208  10  1. 1  24  52  2 . 10  620  570  39137  0146  3  1040  99  8  1. 0  21  32  1  04  460  360  39138  0146  7  2100  129  12  1. 1  20  25  1 .4 4  640  275  3 9 1 3 9  0 1 4 6  10  1090  48  9  0. 5  14  28  1 .5 5  560  215  3 9 1 4 0  0146  16  1890  144  15  1  4  20  39  2 .90  580  340  3914 1  0146  34  1430  143  10  i:  2  21  36  1 .6 9  600  340  39  0 1 4 6  12  2780  132  18  0. 6  19  31  2 . 73  600  460  134  142  39143  0 1 4 6  36  1290  70  12  0. 6  14  27  1 .GO  740  262  39144  0146  18  1850  61  1 1  0. 5  18  39  2 . 58  660  213  3 9 1 4 5  0146  16  1550  7 1  9  4  18  4 1  1 .5 7  560  233  3 9 1 4 6  0 1 4 6  270  2660  73  13  39147  60  910  68  14  o.9  0146  39148  0146  27  1480  98  3 9 1 4 9  0146  7  760  66  0  15  30  3. 07  680  245  0. 4  17  38  1 .7 3  740  248  29  0. 7  15  49  2 .88  640  286  14  0  6  17  31  1 .4 7  480  243  MN  10  12  24  260  105  1 1  20  3. 31  380  4 20 530  13  0  4  19  30  1 .0 3  480  196  57  28  0. 5  23  32  1  22  500  6 0 0  109  50  0. 9  16  20  9  360  730  3  162  112  16  0. 6  19  33  0  95  480  940  0146  5  188  189  40  1 .4  15  23  2. 23  460  0146  4  1  0. 4  16  26  1 .4 6  4 20  750  17  22  220  940  321 22 1 5 7  220  380  380  7 20  320  337  081 29 0 7 1 29 0 45 24 0 68  340  680  380  550  340  450  340  3 14  39198  0 1 4 6  3  39199  0 1 4 6  39200  0 1 4 6  3  39201  0146  39202  0146  39203  0  39204  146 0 1 4 6  39205  0146  DDH  F  068  3 9 1 0 8 109  AG  CO  2  127  18 650  65  94  1 1  145  88  275  88  46  139  169  17  2 104 3 230 2 182 3 77 5 14 1  92 92 63 60 57  23 7  7 5  1  1. 3 0. 8  1 14  2  13  5  1 .9  1  7  1 .2 1 .2  7 16  16 14  8 13 .  14 12  20  10  1  55  35  490  109  0 6 9 1600  39206  0146  160  39207  0 1 4 6  170  37B  39208  0  130  315  39209  0 1 4 6  240  120  39210  0146  150  930  3921 1  0 1 4 6  63  1310  146  7  0  5  23  0  4  17  0.  38  15  0. 2  3  0.5 1.4  12 1 1  2 . 7  13  10  1 .9  12  12  55  14  151  12  3 9 2 12  01.46  74  1960  1 18  17  392  0146  72  1310  128  13  176  13  13  39214  0146  75  2 360  392  15  0 1 4 6  2 10  4200  77  392  16  0 1 4 6  180  4000  8 1  39217  0 1 4 6  92  4 400  76  7  39218  0 1 4 6  1 12  3190  58  7  39219  0 1 4 6  26  2070  53  5  39220  0 1 4 6  156  5000 4 150  0 98 8 2 76 7 2 49  19 55 30  10 9  1 2. 9 1. 1 08 8 0 0.6 0  59  5  0  227  9  8  2. 1  10  8 9  13 14  1 1 13  10 1121 1 1 12  13  840 620  76 56  940  94 1 14  1  32  9  1  50  720  9  0  45  840  0  55  900  5  72  940  185 175  0 4 1 900 14 0 66 6 4 0 2 8 2 72 540 1 10 99 10 1 17 8 8 0 1 1 5 12 940 85 1 0146 49 1 236  9  820  800 1 10 58 50 800 10  1.  107 74  186 . 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(8 8 1 14 7 0 . 80 6 1 .32 8 1 50 8 1 47 9 1 .0 0 8 0 61 9 0 80 8 0 . 57 7 0 90 8 1 02 9 1 20 9 0 95 10 0 . 5 9 8 0 67 9 0 96 9 0 .66 8 0 . 7 1 8 0 .67 7 0 . 72 8 0 .80 8 0 53 9 1 . 26 9 0 . 76 1 1 1.08 9 1.64  1400 1220 1300 1300 1 160 1400 1360 1330 960 1360 1 180 1 140 1360 960 10O0 1200 840 1280 1360 1200 1280 880 1020 960 100O 1480 1400 1600 1280 1400 1200 1240 1060 1360 1240 1 180 I2B0 1280 1 120 1000 1 160 1 100 1200 1280 1520 1240  18 15 13 17 13 45 23 23 350 25 64 10 10 580 54 23 2 16 45 20 1 1 7 1 43 46 65 60 93 84 1 1 10 66 56 72 83 55 52 97 79 20 65 53 58 50 20 12 12 1 1  ODH 0 8 8 37340 3734 1 37342 37343 37344 37345 37346 37347 37348 37349 37350 3735 1 37352 37353 37354 37355 37356 37357 37358 37359 37360 3736 1 37362 37363 37364 37365 37366 37367 37368 37370 3737 1 37372 37373 37374 37375 37376 37377 37378 37379 37380  0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0129 0179 0129 0129 0129  330 130 48 26 160 150 330 76 22 23 20 170 25 160 1020 22 66 38 84 56 (4 53 260 20 66 320 14B 98 260 86 1 1 28 4 30 3 1 260 1950 93 230 230 45  84 28 2150 0 114 2 180 17 1 4 38 2910 0 4 0 1760 28 34 6 2350 0 7 29 10 5 1 0 1780 33 3 0 1350 41 6 0 34 1840 3 0. 4 2300 39 0. 7 43 1240 0. 3170 39 6 0. 1 1 0. 1420 40 5 2 180 48 0. 6 2030 55 0. 49 6 1520 0. 7 2130 48 0. 12 45 0. 3500 450O 46 10 0 57 5 1920 0 55 8 2900 0. 6 6100 46 0. 7 1220 43 0. 77 1 1 0. 2850 7 56 0. 1370 4 1 3380 6 0 64 12 10 50 0. 7 38 0. 1070 6 45 2720 0 8 34 1730 0. 7 21 10 72 0 5 65 0. 3800 54 2 0. 1700 5 1870 78 0. 58 5 0. 1890 14 47 0 1670 6 0. 1280 40 74 26 0. 2010 5 3 0 0 1950 1550 3 5 . 74 12 0. 1840  7 1 2 1 1 1 1 1 1 1 1 1 1 1 2 1 1 2 2 1 2 3 1 2 1  2 2 1 1 "1 2 3 1 2 1 1 1 2 0 2  16 18 18 16 15 16 13 13 15 18 16 15 14 15 18 16 16 17 16 15 20 22 18 23 22 21 26 19 18 20 31 18 16 21 19 18 15 19 15 19  36 28 40 30 37 31 31 27 43 42 30 50 3 1 36 35 40 47 38 47 29 45 58 29 53 40 33 31 24 29 23 34 36 27 35 29 25 23 32 27 23  7 700 2 .61 740 1 . 8 3 1040 1 . 10 50O 1 . 80 500 1.80 880 1 . 23 540 1 . 75 780 2 .06 620 1 . 66 760 1.57 560 3 . 75 520 1 . 90 540 2 .60 160 2 .60 520 1 . 55 560 3 . 45 260 3 . 10 720 5 70O 2 *10 340 2 . 99 700 5 600 1 . 40 320 3 . 62 420 1 . 50 380 6 520 1 . 30 BOO 1 . 2 1 4 20 2 . 65 520 1 . 80 540 2 . 13 7 20 3 . 20 700 1 . 49 660 2 . 60 500 2 .04 963 3 OO 640 1 . 39 500 3 7 1 148 185 560 2 . 47 540  860 127 3 1 258 323 G70 2.1 J 2 19 332 278 220 220 192 276 384 2-14 4 10 34 1 344 325 470 208 288 550 280 238 2<I0  237 232 162 3 1 1 287 267 337 32 274 306 700 400 590  DDH 0 0 9 39157 39158 39159 39 160 3 9 16 1 39162 3 9 163 39 164 39165 39 166 39 167 39 168 39169 39 170 39 17 1 39 172 39 173 39 174 39 175 39126 39 127 39128 39 129  0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 014G 0146 .0146 0146 0146 0146 0146  DDH 0 9 2 37427 37428 37429 37430 37431 37432 37433 37434 37435 37436 37437 37438 37439 37440 3744 1 37442 37443 37444 37445 37446 37447 37448 37449 37450 37451 37452 37453 37454 37455 37456  0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146  8 390 4 337 3 400 2 90 3 61 2 132 5 200 4 138 3 186 179 3 4 650 5 145 3 1080 4 420 3 580 6 304 3 680 3 245 2 196 2 180 3 139 2 328 5 1040  180 240 310 820 400 230 690 4 10 76 3 10 280 96 180 56 114 51 4 1 63 63 89 2 10 430 80 160 600 320 92 74 104 35  14 10 1520 1530 1400 1460 1330 1750 1440 880 1070 1280 90O 1200 2370 1360 26 10 2690 6250 350O 6150 3240 3590 2470 3360 3470 1900 2570 2640 4100 28BO  103 90 148 120 68 85 203 204 37 7 1 304 240 520 57 48 29 28 3 1 26 34 27 35 142  1 1 8 7 27 2 4 3 16 3 9 134 116 255 6 7 6 3 3 2 8 6 6 10  1 .6 0 .6 1.0 2 .6 1.0 1.9 1. 1 1.0 0 .5 0 .3 2. 4 2. 1 4 .4 0 . 4 0 . 2 0 . 2 0 . 2 0 . 2 0 . 2 0 .2 0 . 2 0 . 2 1. 1  65 134 362 84 77 30 164 32 76 40 1 14 49 43 124 31 131 88 67 160 124 180 68 87 70 83 78 50 62 68 54  13 6 9 12 6 6 6 8 20 10 10 10 1 1 7 7 44 7 10 12 30 37 18 9 9 23 9 6  1. 2 2. 7 5 8 1 7 1. 1 0 .4 2 1 0. 6 1 .2 . 1 .0 1 .7 1 .0 1 .5 0. 9 0 6 1 .0 0 4 0. 6 0 8 0. 9 1. 6 0. 5 0. 4 0. 3 0. 5 0. 5 0. 3 0. 4 0. 4 0. 3  to  15 8  64 8 1 32 20 20 17 18 20 16 14 14 23 19 23 2 1 16 13 14 14 12 13 13 20  13 15 17 15 15 14 14 15 15 15 14 14 14 48 28 7 1 20 18 16 24 23 29 91 102 98 68 21 20 20 23  40 47 23 19 24 17 2 1 18 26 22 1B 22 25 40 37 29 22 23 25 23 17 28 29  0 . 5 1 0 . 43 0 .30 0 . 38 0 . 2 1 0 .23 0 . 25 0 . 76 0 .24 0 . 48 1 1 0 .95 18 0 .57 . 94 0 0 .52 0 . 74 0 . 32 0 . 34 0 . 27 0 . 17 0 . 43 1 .57  600 880 880 580 640 500 480 460 420 440 560 560 860 560 4 60 560 480 360 620 400 500 500 620  134 227 234 206 181 105 243 380 190 275 289 210 324 287 304 143 108 123 117 150 107 173 294  9 2 . 1 1 800 170 15 2. 18 780 253 22 1 .0 5 860 500 12 1 .3 0 199 820 12 1 .52 1 160 15 13 '1! 1 .0 0 1060 12 1 .23 249 880 10 0 . 75 840 165 12. 1. 45 800 201 M ' O . 64 1000 16 1 1 1. 1.1 164 920 10 0 . 86 920 100 10 .1. 70 660 150 32 2 . 83 1080 33 14 1 .65 1300 . 14 4 0 3 . 95 1060 50 34 2 . 7 0 540 330 35 9 840 220 35 3 . 8 0 880 380 52 13 680 370 44 3 . 99 740 282 45 12 680 4 10 46 2 . 97 720 450 8 5 1 287 880 45 9 1000 35 33 2 . 86 29 1 660 39 3 . 5 0 740 340 32 3 . 97 340 289 32 3 . 78 640 231 38 3 . 1 1 5 2 0 264 1  37457 37458 37459 37460 37461 37462 37463 37464 37465 37466 37467 37468 37469 37470 3747 1 37472 37473 37474 37475 37476 37477 37478 37479 37480 3748 1 37482 37483 37484 37485 37486 37487 37488 37489 37490 37491 37492 37493 374 94 37495 37496 37497 37498 37499 37500 39101 39 102 39103 39104 39105 39106 39107  0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146 0146  4 1 52 290 150 120 150 50 74 53 102 143 60 8 1 390 2 10 1 10 260 95 130 130 60 540 133 270 72 170 82 56 240 240 75 28 86 93 83 17 94 2 10 120 260 220 430 190 7 1 3 10 230 48 1080 800 140 250  2370 3040 40OO 2710 2980 2720 4050 5150 8700 3320 2050 15BO 1540 2250 1800 3050 2250 2 1O0 2730 5850 2070 4750 60O0 2970 2920 2500 2600 3420 2720 2300 3560 4250 4200 1720 3200 2 120 1250 2080 3270 2620 1930 1220 2300 3400 2720 2860 1920 1350 1860 1810 2470  63 47 47 38 79 25 54 64 49 31 27 23 30 21 18 14 21 26 23 46 21 76 38 58 77 69 63 68 40 33 60 78 140 105 83 12 1 33 59 57 34 IB 21 33 64 7 1 160 20 23 20 297 339  6 8 8 7 12 6 7 1 1 12 6 8 13 17 5 5 4 5 13 B 5 5 5 6 5 4 3 5 7 4 3 6 9 7 9 9 18 6 6 7 6 3 6 6 7 5 16 9 10 7 126 145  0. 3 0. 2 0. 2 0. 3 O. 8 0. 2 0. 4 0. 6 0. 5 O. 3 0. 2 O. 2 0. 2 0. 2 0. 2 0. 2 0. 2 0. 2 O. 2 0. 3 0. 3 0. 4 0. 4 0. 5 0. 5 0. 4 0. 5 0. 4 0. 3 0. 2 0. 4 0. 3 1 3 0 9 0 .6 0 9 0 . 3 0 . 3 0 . 3 0 .4 0 . 2 0 . 2 0 . 2 0 . 2 0 . 2 1 .9 0 .3 0 .4 0 . 2 3. 8 4 .5  26 2 1 17 17 16 14 18 2 1 17 16 15 12 11 13 1 1 9 10 15 12 4 1 12 13 39 38 53 51 20 14 12 1 1 15 17 14 13 18 14 10 18 15 13 1 1 12 55 96 73 19 12 12 14 10 1 1  38 2 . 52 33 3 . 38 26 3 . 97 25 4 . 13 27 4 . 18 23 2. 5 0 25 8 26 10 23 14 25 8 18 2 . 74 12 2 . 41 9 1 .5 9 14 2. 92 1 1 2 74 12 7 1 1 2 .51 10 2. . 5 3 13 3 0 3 33 10 18 2 82 19 8 28 12 28 3 . 5 5 37 3. 98 32 3 0 3 24 3 . 5 4 22 7 16 6 14 3 . 4 6 20 7 28 7 23 8 15 3 . 0 1 38 3 . 22 2 1 3 OO 14 2 .OO 24 2 . 9 7 20 8 17 3 . 2 0 13 2 . 4 8 13 2 . 3 8 26 2 . 9 9 48 10 36 3 . 15 28 3 . 6 3 16 3 . 9 7 10 2 . 5 7 15 i . 86 14 17 t 1 36  380 *480 600 720 720 720 640 720 780 lOOO 620 840 760 SOO 920 660 840 1500 980 1080 840 1000 1120 1200 1360 1600 130O 1000 920 640 820 860 860 70O 640 580 660 500 700 740 680 720 680 1 120 880 800 720 880 940 780 740  340 219 223 137 163 122 224 180 153 16 147 95 82 102 65 42 50 79 81 14 40 1 1 18 17 22 25 22 2 1 1 12 1 12 194 260 193 252 248 250 151 230 222 105 99 8 1 155 25 266 276 1 11 233 1 i 1 154 128  DDH 0 9 2 39230 39232 39234 39236 39238 39240 39242 39244 39246 39248 39250 39476 39478 39480 39482 39484 39486 39488 39490 6 7 901 67903 67905 67907 67909 6791 1 67913 67915 67917 67919 6792 1 67923 67925 67925 67927 67929 6793 1 67933 67935 67937 67939 6794 1 67943 67945 67947 67949 67951 67953 67955 67957 67959 67961 67963 67965 67967 67969 67971 67973 67975 NIMG 37235  1 ) CONTINUED  66 .84 54 . 0 3 66 . 8 9 65 85 66 22 66 06 67 12 64 . 9 3 65. 70 67 6 5 58 21 70 20 5 5 78 68 . 15 68 9 5 6 9 45 69 06 67 33 73 33 58 56 59 . 9 0 57 0 5 6 0 49 7 1 35 7 0 . 62 68 31 57 08 5 9 48 61 52 68 0 9 6 1 35 6 1 65 65 . 67 66 27 6 5 78 67 . 19 69 34 57 65 58 72 58 1 1 62 8 9 7 0 .44 68 01 67 77 75 17 6 0 38 6 9 33 68 8 0 68 35 68 93 71 14 69 83 69 53 6 9 48 66 47 61 . 4 8 6 5 . 25 58 19 73 . 6 2 66 . 72  17 17 16 16 16 15 16 17 16 17 16 14 20 17 15 15 16 17 14 15 15 14 15 13 14 14 15 16 15 17 16 15 15 17 16 17 16 14 15 16 15 15 15 3 18 17 17 17 17 17 16 16 15 16 16 16 16 20 13 17  . 18 .59 13 38 .25 .99 20 .20 82 15 73 .34 71 14 55 33 66 32 69 77 38 89 48 . 29 . 37 . 12 .07 .09 . 33 .71 .50 .52 . 33 . 24 . 37 .00 94 91 88 26 73 .54 .45 .46 66 31 91 49 95 32 .60 97 .92 .94 .88 .85 .65 .29 .55 .06  3 .07 3 .63 3 .44 5 . 18 5 .45 4 .37 3 .47 6 .51 5 .48 2. 56 4 .60 4 . 62 14 94 4 . 55 3 . 24 4 13 3 17 3 91 1 . 70 a 71 9 04 a 90 7 .77 0 98 1 33 1 . 29 a .27 7 80 6 .44 3 01 7 .04 6 . 48 4 .94 6 94 3 . 58 3 58 3.. 0 6 9 43 10 . 9 6 10 . 17 8 92 3 .02 2 22 6 .94 3 30 12 37 3 . 16 4 99 7 81 6 . 40 4 26 3 64 3 .45 3 .65 5 58 8 08 5 .24 15 OO 2 .08 3 98  3 .48 1 .33 2 13 1 .04 1 . 0 5 16 . 6 0 2 93 3 87 1 86 1 .74 3 21 2 62 2 10 3 . 33 2 32 3 .28 2 59 2. 89 1 56 2 61 3. 31 1 .32 3 .44 0 48 1 60 4 00 0 65 3 .4 1 2 26 1 46 2 . 4 8 12 . 7 0 0 05 1 08 1 52 0 . 11 3 29 1 .54 1 16 4 41 O 83 0 .31 1 98 3 18 0 .48 3 .09 1 21 0 32 1 .07 4 14 1 .61 1 . 15 3 . 38 2 98 0 74 0 . 72 0 . 6 5 4 .97 5 .56 2 50 5 .07 3 .93 2 31 1 92 7 .53 5 02 4 .86 2 .57 3 84 1 .43 2 . 38 1 .38 3 .04 1 ,00 1 .40 1 .41 4 .51 1 81 6 .09 5 .81 2. .02 4 .99 4 .95 2 40 3 . 33 5 . 23 3 33 1 .30 2 . 7 1 1 .. 16 3 .83 5 . 25 1 96 3 .20 5 27 3 08 2 .90 2 53 3 28 1 .66 2 18 0 38 1 .95 4 . 54 2 35 1 00 3 . 94 2 . 19 1 25 3 60 0 18 2 . 39 9 . 4 0 . 0 . 82 7 . 45 2 . 40 0 09 4 16 0 56 6 76 5 .05 1 .44 0 17 1. 22 1 .46 0 36 1 .49 2 7 1 2 45 2 .22 0 .38 0 . 73 0 .88 0 08 0 . 27 0 52 1 .48 3 89 1 .23 0 . 14 1 62 0 . 14 0 .89 2 27 1 15 0 05 0 . 18 O .90 0 .07 O. 84 0 86 0 .07 0 . 94 0 85 0 1 1 1. 93 3 . 48 1 .56 0 51 1 25 3. 0 5 0 28 2 .50 3 . 10 0 . 91 4 82 0 50 2 30 3 . 15 2 1 1 2. 68 1 . 27 0 . 34 1 .47 0 10 0 84 2 . 79 1 . 24 3 64 2. 66  5 20 5 79 3 49 3 75 3 23 3 50 4 53 5 71 5 09 4 80 4 79 5 86 3 70 3 48 4 85 4 60 2 85 3 27 5 70 2 61 2 68 3 27 3 19 6 24 5 93 6 28 4 03 3 13 2 59 5 64 3 12 2 63 3 59 4 50 4 20 4 27 4 60 3 46 3 22 2 98 4 26 6 15 6 02 1 1 37 1 18 3 16 6 08 4 84 4 15 4 as 4 92 5 64 3 91 4 27 3 47 4 80 3 82 4 62 4 27 3 96  .53 .35 .54 .74 .51 .58 0 .49 0 .45 0 .43 0 .48 0 .56 0 26 1 .20 0 63 0 .50 0 .47 0 .64 0 .57 0 .30 1 .08 1 . 19 0 97 1 .23 0 .29 0 . 30 0 .32 1 . 17 1 .05 1 .09 0 .42 0 90 1 08 0 . 76 0 69 0 74 0 59 0 . 54 1 04 1 . 12 1 07 0 . 91 0 . 41 0 42 1 33 0 . 34 1 .26 0. 60 0 48 0 . 50 0 . 47 0. 40 0 46 0 . 51 0 . 50 0 . 76 1 22 0 . 75 0 . 78 0 . 10 0 . 52 0 0 0 0 0 0  0 27 0 . .74 0 . 19 0 . 24 0 18 0 . 19 0 14 0 16 0 . 17 0 16 0 . 16 0 17 0 . 32 0 .22 0 15 0 14 0 . 17 0 . 14 0 13 0 19 0 . . 17 0 15 0 . . 17 0 . 13 0 . 12 0 . 15 0 . 20 0 . 20 0 . 57 0 . 16 0 . 22 0 . 63 0. 09 0 . 23 0 . 19 0 . 15 0. 1 1 0 . 32 0 . 18 0 . 22 0 . 22 0 . 17 0 . 17 0 . 18 0 06 0 . 17 0 . 10 0 . 14 0 . 14 0 . 13 0 . 08 0 . 20 0 . 13 o . 18 0 . 2C 0 . 31 0 . 24 0 . 26 0 . 01 0 . 18  37458 37205 39265 37486 39184 37448 37500 37412 37482 37325 37352 37374 37399 39240 39137 37399 37297 37308 37318 37226 39132 39163 39157 39157 67916 39173 37419 37233 37431 37276 37253 67920 67969 67933  59 67 66 65 62 56 47 67 51 66 60 56 65 66 61 67 67 67 67 67 60 68  55  55 67 62 68 66 69 70 66 67 66 69  r  25 23 68 87 05 53 .08 93 . 10 .93 38  .00  . 14 19 25 47 20 33 16 48 70 85 .93 81 58 65 98 48 . 11 88 37 .53 . 44 .98  16 15 16 16 16 16 15 14 16 17 16 16 15 15 16 14 17 14 17 15 16 17 14 13 16 16 13 15 16 12 16 16 16 16  73 51 79 26 70 79 26 31 57 65 14 55 30 88 33 72 53 95 48 95 22 04  OO 71 71 33 86 73 94 6 / 93 49 88 87  5 .22 9 .03 2 .31 3 82 2 .08 4 27 1 63 4 08 8 21 4 .98 5 OO 9 .78 10 . 8 9 12 . 5 1 1 .80 1 .42 8 64 9 . 14 1 .56 2 .21 3 .86 8 .17 5 .39 9 .57 3 86 3 . 16 2 .53 4 29 5 86 9 39 3 03 2 11 4 46 1 .84 3 56 1 75 2 41 2 98 2 46 3 .46 5 89 io .43 6 19 1 82 1 1. 6 2 10 . 9 6 6 3 11 35 11 1 57 3 . 18 8 .71 4 88 1 01 1 33 4 Ol 1 94 1 .29 3 06 2 . 15 1 75 5 . 13 1 88 1 .40 3 35 2 61 5. 57 1 .6 3 3 08  4 .41 1 88 3 . 19 4 .58 2 .22 7 .77 7 .65 4 .25 7 .38 6 .30 6 06 6 88 3 .33 3 .31 2 .72 2 .81 2 .21 2 52 5 02 1 .29 1 .74 0 . 89 1 29 1 27 3. 31 2 77 3 87 2. 71 1 93 2 82 3 52 3 09 0 91 2 72  1 .30 3 .75 2 19 2 54 0 91 1 13 0 .77 1 60 1 54 O 37 1, 27 2 .56 1 .91 2 .94 1 .21 2 08 0 66 3 59 0 . 12 3 85 0 . 07 0 . 31 0 . 62 0 51 3. ,79 0 87 2 19 4 27 1 40 2 52 0 . 96 4 .0 9 3 08 0 11  3 .34 3 .76 3 .95 3 .58 3 .99 2 .45 5 .29 6 54 5 30 4 .61 2 .95 2 .27 5 .68 3 .46 2 .09 5 .72 5 .63 4 45 4 39 3 97 3 48 3. 84 3 69 3 71 2 .83 2 .61 6 .29 3 . 16 5 .44 3 .95 4 46 2 .82 3 46 4 .47  1 .0 3 0 . 56 0 . 52 0 . 80 1. 02 0 97 o 99 0 35 1. 0 5 o. 43 0 . 96 1. 11 0 . 62 0 57 1 . 12 0 .55 0 50 o 45 0 . 41 o. 56 1. 11 0 . 72 1. 12 1. 12 0 52 0 95 0 32 o 63 0 .38 0 35 0 55 0 52 0 76 0 54  0. 1 0 . 18 0 . 18 O. 2 9 O. 14 0 . 18 0 21 0 . 15 O. 29 O. 18 0 . 22 0 . 19 O. 16 O. 19 0 14 0 . 15 0 17 O. 10 O. 14 O. 16 O. 35 O. 0 9 O. 22 0 . 23 0 . 12 o 21 o. 15 o. 18 o 14 0 . 14 0 . 15 o 15 0 . 18 o. 11  ss- 1 ss- 2 ss- 3 ss- 4 ss- 5 ss- 6 ss- 7 ss- 8 ss- 9 s s - 10 ss- 1 1 5S- 12 s s - 13 s s - 14 s s - 15 s s - 16 s s - 17 s s - 18 55- 19 s s - 20 s s - 21 s s - 22 s s - 23  0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152 0152  19 240 240 90 98 123 106 91 71 220 100 31 26 129 190 230 290 390 260 280 170 180 160  520 680 680 313 335 374 402 339 344 365 315 228 237 720 610 550 540 710 370 750 530 570 500  590 100 105 165 178 91 270 213 166 145 315 302 250 120 121 124 131 130 124 125 113 120 113  1 18 97 102 103 117 128 159 1.14 105 127 185 226 208 134 170 227 289 206 346 243 193 190 184  3. 6 0. 9 0. 4 0. 5 0. 5 0. 6 11 . 0. 6 0. 3 0. 6 0. 8 0. 8 0. 7 0. 6 0. 5 0. 5 0. 6 0. 5 0. 6 0. 5 0. 4 0. 5 0. 4  31 21 20 12 13 15 17 15 1 1 17 14 12 14 15 15 16 18 16 14 17 16 15 15  36 17 17 12 13 14 16 13 12 15 17 15 14 18 19 19 26 22 20 24 19 19 18  2 .3 1.8 1.8 1.9 2. 1 2 .3 2 .3 2 .2 1.8 2 .9 2 .4 2 .3 2. 5 1.8 3 .8 5 8 7 .0 4 .9 6 .0 6. 3 2 .9 3 .5 3 .5  320 880 700 640 640 580 440 620 760 780 960 620 760 840 660 640 520 600 380 560 360 480 500  910 155 148 160 187 196 257 186 137 140 174 450 400 260 274 257 380 400 224 338 218 255 238  10% HCL ID.NO  NH40X  EXT.  ID.NO  LOCATION CA  CU  FE  EXT  LOCATION  MO  CA  CU  0 446 446 0 223 o 0 0 O o 0 0. 0 0 0 o 0 0 0 0 0 0 0 o 0 0 0 o 0 21 8 6 8 2 1 868 21 8 6 8 25 5 1 3 2 1 .8 6 8 18 2 2 3 21 . 8 6 8 18 2 2 3 28 6 0 3 3 5 . 754 28 6 0 3 25 0 2 8 17 8 7 7 0 .0 25 . 0 2 8 2 1. 4 5 3 28 6 0 3 28 6 0 3 28 . 6 0 3 0 0 0 .0 17 8 7 7 21 4 5 3 32 . 179 35 . 754 39 330 42 . 9 0 5 57 207 42 . 9 0 5 18 223 14 579 0 0  0. 0 104 . 712 157 0 6 8 171 7 2 8 167 . 5 3 9 1.15. 183 4 . 168 4 . 188 4 . 188 10 47 1 10 471 16. 7 5 4 8 . 377 O. 0 12 5 6 5 0. O 2 5 . 131 20 888 16. 7 1 0 22 9 7 7 12 5 3 3 10 444 41 7 7 5 20 888 4 1 .775 84 9 7 4 124 . 3 5 2 51 8 1 3 45 5 9 6 20 725 0 .0 24 B 7 0 10 3 6 3 10 363 8 .290 16 . 5 8 0 0 .0 0 .0 8 . 290 12 4 3 5 10 . 3 6 3 12 4 3 5 10 3 6 3 12 . 4 3 5 a 290 16 5 8 0 12 . 5 6 5 12 . 5 6 5 16 . 754  FE  MO  ODH 0 7 8 37226 37227 37228 37229 37230 37231 37232 37233 37234 37235 37236 37237 37238 37239 37240 37241 37242 37243 37244 37245 37246 37247 37248 37249 37250 37201 37 202 37203 37204 37205 37206 37207 37208 37209 37210 3721 1 37212 37213 37214 37215 37216 37217 37218 37219 37220 37221 37222 37223 37224  0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  912 .585* 0 .375 595 164 0 . .234 0 .250 2777 .433* 0 . 5 4 6 2 8 1 7 . 1 12* 0 .500 3273 .405* 5 9 5 . 164 0 937 13 . 8 8 7 1 .951 1 1. 9 0 3 1 .561 15 .871 . 2 .279 1 1. 9 0 3 2 .341 21 . 8 2 3 2 . 154 39 . 6 7 8 2 .498 1 1. 9 0 3 2 .279 1 1. 9 0 3 1 .717 1 1. 9 0 3 1 .467 17 . 8 5 5 2 .373 67 . 4 5 2 3 .434 2 .238 32 . 8 9 0 1 . 190 40 .629 69 .649 1 508 1 .587 46 . 4 3 3 3 .365 48 . 3 6 8 50 .302 2 .349 42 . 5 6 3 2 . 777 108 . 343 2 .539 1 .940 172 . 9 7 3 12 1 . 8 6 7 0 .782 68 . 796 0 .861 1 .111 78 . 6 2 4 39 312 0 .626 1 221 9 828 39 . 3 1 2 1 .721 27 518 1 . 768 35 381 1 252 1 . 440 35 .381 2 9 . 484 1 .377 1 .596 15. 725 1 .017 23 587 4 068 1 1 794 27 518 2 159 1 .596 31 4 5 0 23 587 2 285 1 643 35 381 285 2 31 4 5 0 23 587 2 175 . 5 0 2 35 1 381 35. 710 1 . 124 1 .0 9 3 25. 790 45 6 2 9 1 .436  0 .424 0 . 297 0 . 318 0 278 0 . 221 0 .242 0 259 0 257 0 231 0 .. 2 4 0 0 ..233 0 .265 0 371 0 ..246 0 .225 0 .. 2 4 8 0 . 382 0 313 0 296 0 222 0 . 186 0 .317 0 .482 0 .573 0 .406 0 .201 0 . 183 0 . 186 0 135 0 . 186 0 . 142 0 2 10 0 . 175 0 . 37 1 0 . 223 0 . 197 0 . 240 o.227 0 . 917 0 . 448 0 . 245 0 . 306 0 . 186 0 . 382 0 . 188 0 . 170 0 . 227 0 . 174 0 . 201  4 0 . 100 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 o 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 o 0 .0 0 .0 0 .0 0 .0 0 0 0 0 0 .0 0 0 0 0 0. 0 0 0 0 0 0 0 0 .0 0 0 0. 0 0. 0 0 0 0. 0 0. 0 0 ..0 0. 0 0. 0  37226 37227 37228 37229 37230 37231 37232 37233 37234 37235 37236 37237 37238 37239 37240 37241 37242 37243 37244 37245 37246 37247 37248 37249 37250 37201 37202 37203 37204 37205 37206 37207 37208 37209 37210 3721 1 37212 37213 37214 37215 37216 37217 37218 37219 37220 37221 37222 37223 37224  0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 O O 0  o o  0 0  o 0 0  o o 0  o 0 0 0  o o o 0  o 0 0 0 0 0  o  o  0 0 0  o  0  0  0 0 0  o o 0 0  o 0  o 0 0  o 0  o 0  o 0 0 0 0 0  o o 0 0  o o 0  o 0 0 0 0  o 0 0 0 0 0 0 0 0 0  0. 36 36 0. 18  0. 0 0 . 134 0 . 068 0 038 0 . 038 0 119 0 293 0 . 457 0 276 O. 174 0 144 0 142 O. 7 6 5 0. 0 0. 038 O. O 0 OI3 0 . 054 0 . 172 0. 056 0 .064 0 043 0 032 0 034 0. 077 0 069 0 .088 0 076 0 .042 0 074 0. 0 0 076 0 069 0 164 0 078 0 067 0 .0 0 .0 0 .526 0 .072 0 .069 0 .048 0 .021 0 055 0 . .02 1 0 084 0 . 068 0. 049 0. 059  0. 0 0 0 0 ..0 0. 0 0. 0 0 0 0 0 0. 0 0 0 0 0 0 0 0 0 0 0 o 0 0 0 o 0 0 0 0 0 o 0 0 0 0 .0 0 0 o 0 0 .0 0 0 0 .0 0 .0 0 o 0 .0 0 o 0 .0 0 o 0 .0 o .0 0 .0 0 .0 0 .0 0 .0 o .0  o o  0 .0 0 .0 0 .0 0 o 0. 0 0 .0 0 0 0. 0 0 .0  KCL03 ID.NO  37226 37227 37228 37229 37230 37231 37232' 37233 37234 37235 37236 37237 37238 37239 37240 3724 1 37242 37243 37244 37245 37246 37247 37248 37249 37250 37201 37202 37203 37204 37205 37 206 37207 37208 37209 37210 372 1 1 37212 37213 37214 37215 37216 37217 37218 37219 37220 37221 37222 37223 37224  EXT.  HN03.HCL04  LOCATION  0 0 0 0 0 0 0 0 O 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  ID.NO CA  CU  0. 0 5 6 9 . 839 9 2 5 . 988* 169 1 .7 0 9 * 747 . 9 1 3 1 9 5 8 . 82 1 • 142 . 4 6 0 178 . 0 7 5 2 4 0 . 401 169 . 17 1 281 . 358 9 4 3 . 796* **•****#• 1 .781 O O. 0 2 4 2 . 181 266 . 984 0. 0 0 0 572 . 1 10 1 2 4 6 . 5 2 2 * 568 . 207 477 . 064 532 . 1 10 195. 801 78 1 1211. 009* 291 . 6 2 3 . 853 276 . 425 954 129< 5 6 0 . 528 476 . 0 6 5 1064 220* 743 . 1 19 6 3 3 474 69 1 .062 1798 165* 6 18 731 153 1 53 1 * 5 1 0 453 144 1 4 4 0 * 464 0 4 8 1009 0 0 8 * 425 . 378 1603 . 6 0 3 * 897 . 160 5 9 0 .991 0 .0 0 .0 560 . 360 8O0 . 483 699 .099 587 795 403 . 6 0 4 1005 . 4 3 8 345 . 9 4 6 440 .846 338 739 5 9 9 . 396 O .0 0 .0 0 0 0 .0 3 2 8 7 . 0 0 8 * 135 . 135 4 14 .4 14 . 580 .060 378 . 378 394 .441 486 . 4 8 6 6 3 0 . 332 724 . 324 386 . 7 0 7 5O0 .901 785 . 0 1 5 515 3 t 5 96 . 6 7 7 666 .667 533 656 4 2 0 . 256 488 . 200 644 . 6 3 0 675 .089 6 7 3 . 122 411 . 9 1 9 0. 0 22 . 884 19. 0 7 0 83 . 909 9 9 . 166 1 3 3 . 492 4 0 0 . 477 324 . 195 457 . 688 404 . 291 3 5 0 . 894 4 19 . 547  6  FE 0. 0 1 . 121 1 .578 1 .91 1 1 .205 1 .454 1 .931 1 .495 1 .205 1 765 1 .703 1 .391 2 .035 O. 0 3 904 0. 0 2 492 1 .253 1 .232 2 259 1 478 2 177 1 273 0 .945 1 745 2 707 2 . 4 15 2 311 2 . 186 2 . 207 1 . 791 1 . 895 0 .999 1 .707 1 .916 2 .041 O .0 0 .0 1 .624 1 . 832 1 770 1 .770 3 123 1 .583 1 645 1 .478 1 .661 1 .412 1 . 495  CA  MO 0. 0 86 . 300 185. 545 336. 570 47 . 465 107 . 8 7 5 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 22 . 936 27 . 523 82 . 569 91 . 743 1 14 .679 91 743 137 615 37 . 209 23 . 256 23 256 6 0 . 465 0 .0 0 .0 23 . 2 5 6 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 23 . 2 5 6 55 . 8 1 4 32 . 5 5 8 23 . 256 41 . 8 6 0 55 . 8 1 4 0 .0 21 . 575 496 . 2 2 5  EXT  LOCATION  37226 37227 37228 37229 37230 37231 37232 37233 37234 37235 37236 37237 37238 37239 37240 37241 37242 37243 37244 37245 37246 37247 37248 37249 37250 37201 37202 37203 37204 37205 37206 37207 37208 37209 372 l O 3721 1 3 7 2 1Q 37213 37214 37215 37216 37217 37218 37219 37220 3722 1 37222 37223 37224  O 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0  o 0 0  0 0 0 0 0  o  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o  o o  o  o  0 0 0 0 0 0 0 0 0 0 0  0  0 0 0 0 0  o 0 0 0 0  0 .0 14 . 0 1 2 14 . 0 1 2 17 . 5 1 5 22 . 7 7 0 26 . 273 38 . 5 3 3 64 . 806 5 0 . 794 26 . 273 17 . 5 1 5 17 . 5 1 5 7706 . 6 2 5 * 0 .0 10 . 509 O .0 26 . 273 35 . 9 9 6 28 . 796 23 . 397 25 . 197 21 . 5 9 7 16 . 198 37 . 795 242 . 9 7 0 55 . 0 4 6 504 . 587 275 229 36 697 6 0 9 . 174 0. O 284 404 233 0 2 7 1467 . 8 9 0 * 2 4 9 . 541 201 . 8 3 5 0 O 0. 0 6 7 8 . 899 3 6 . 697 45 8 7 2 27 . 523 23 . 8 5 3 18 . 349 2 0 . 183 1 1 3 . 761 2 8 0 . 241 476. 410 154 . 133  CU 0 .0 25 . 0 5 6 29 . 5 3 0 62 . 6 4 0 25 . 0 5 6 59 . 0 6 0 4 . 474 6 . 264 8 .054 6 . 264 7 . 159 26 . 8 4 6 0 .895 0 .0 8 .054 0 .0 38 . 4 7 9 16 . 0 5 4 15 . 162 32 . 9 9 9 19 . 6 2 1 29 . 4 3 1 31 . 2 15 22 . 297 53 512 34 703 4 0 . 183 27 397 4 9 . 315 15. 525 0. 0 10. 0 4 6 14 . 6 1 2 8 . 219 8 . 219 8. 219 0. 0 O. 0 2 . 740 10. 0 4 6 8 2 19 10. 0 4 6 21 . 0 0 5 10. 959 io. 9 5 9 13 . 6 9 9 1 1 6. 3 3 15. 213 2 1 .477  FE 0.0 0.089 0.077 0 . 130 0 . 106 0 . 135 , 0 . 101 0 083 0 . 101 0.097 0 . 102 0 . 123 0.226 0.0 0 . 122 0.0 0.119 0.073 0.074 0.114 O . 109 0 . 1 16 0.090 0.085 0 . 102 0 179 0 169 0 . 137 0 . 132 0.093 O O 0.074 0.116 0.083 0.081 0.098 0.0 0.0 0 . 1 10 0.083 0 058 0.092 0 093 0.067 0.08 1 0 081 0.059 0O65 0.066 1  MO  0.0__ 0.0 13.873 23.121 O O 11.561 0 0 0.0 0.0 0.0 0.0 0.0 0 0 0.0 O O 0.0 0.0 0 0 O O 0 0 0.0  oo oo  0.0 0.0  oo oo oo oo  0.0  oo oo  0.0 0.0  oo o o 0.0  oo  0.0 0.0 0.0 0.0 0.0 0.0 0.0  o o 0.0  o.o  1 1 .561  NH40X  10% H C L E X T . ID.NO  LOCATION  ID.NO CA  37251 37252 37254 37255 37256 37257 37258 37259  ro I  37260 37261 37262 37263 37264 37265 37266 37267 37268 37269 37270 37271 37272 37273 37274 37275 37276 37277 37278 37279 37280 37281 37282  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  1 . 127 2 .031 1.936 0 .968 1 286 0 .968 0 .984 1. 397 1 . 174 1 .778 1 .476 1 .984 1 .995 1 .788 2 .217 1 .862 1 .537 1 . 389 1 .567 1 .848 1 . 182 1 . 774 1 . 774 1 . 301 1 .478 1. 389 1.508 1 .862 2 .542 1 .626 1.995  CU 1 7 4 .. 1 2 3 65 .780 58 .041 73 .519 75 .453 5 4 . 172 54 . 172 48 .368 46 .433 2 7 .. 0 8 6 52 . 2 3 7 34 .825 28 : 2 8 3 24 .. 2 4 2 56. 566 16 1 6 2 80 .808 109 .091 46 .465 88 .889 64 .646 60 .606 90 .909 52 .525 76 .768 52 . 5 2 5 50 .505 60 .606 96 .970 1 17. 172 50 .505  FE 0 . 152 0. 207 0 .. 2 0 3 0 . 194 0 . 199 0. 207 0 . 158 0 . 175 0 . 131 0 . 123 0 . 158 0 . 211 0 . 146 0 . 167 0 . 150 O . 188 0 . 271 0. 282 0 . 251 O . 192 0. 267 0. 240 0 . 261 0 . 324 0. 209 0. 240 0. 292 0. 205 0. 330 0 .. 2 9 9 0 .. 2 1 3  EXT LOCATION  MO 0 .. 0 0 0 0. 0 0 .. 0 0. < 3 0 .0 0 .0 0 .0 0 .. 0 0 .0 0 .0 0 0 0 0 0 .0 0. 0 0. 0 0 0 0 0 0, 0 0 . .0 0 .. 0 0 .0 0 . .0 0 0 0 . .0 0 .0 0 . .0 0. 0 0 0 0 0 0 .0  CA  37251 37252 37254 37255 37256 37257 37258 37259 37260 37261 37262 37263 37264 37265 37266 37267 37268 37269 37270 37271 37272 37273 37274 37275 37276 37277 37278 37279 37280 37281 37282  O O 0 0 O 0 O O 0 O 0 0 0 0 O O 0 0 0 O O 0 0 O O 0 0 0 0 0  o  o 0 0 0  o  0 0 0 0 0 0 0 0 0 0 0 0 0  o o o o 0 o o 0 0  o 0 0 0  18 . 2 2 3 0 .0 0 O 18 . 2 2 3 21 . 8 6 8 18 . 2 2 3 25 .513 21 . 8 6 8 2 9 . 157 2 1. 8 6 8 32 . 8 0 2 2 9 157 O .0 0 .0 0 .0 O O 0 .0 0 .0 0 .0 23 259 0 .0 0 .0 0 0 19 3 8 2 O O 0 0 23 259 19 3 8 2 0 0 0 0 O 0  CU  87 25 27 54 27 27 29 27 31 16 27 22 16  FE  . 729 .065 . 154 . 308 . 154 . 154 . 243 . 154 . 332 . 7 10 . 154 .977 .516 .645 .710 . 387 .032 .710 387 903 516  O 0 0 O 0 0 0 0 0 O 0 O 0 0 0 0 O 0 0 O 0  0 .0 24 . 7 7 4 8 258 20 645 12 3 8 7 8 258 28 9 0 3 43 3 5 5 43 355 22 . 7 1 0  0 0 0 0 0 0 0 0 0 0  20 22 12 33 22 12 28 16  .030 .034 043 .036 .036 .041 028 .034 .013 .017 .021 .058 .037 035 031 050 .091 .070 .079 .037 083 0 .035 058 058 097 .058 039 . 105 .058 050  MO 0 0 O O 0 0 0 O O O O 0 0 0 0 0 O O O 0 O 0 0  ro  0 .0 0 .0 0 .0 .0 0 .0 .0 .0 .0 0 0 0 .0 .0 0 0 0 0 .0 0 0 0 0 0 0 0. 0 0 0. 0 0 0  o o o  KCL03 ID.NO  HN03:HCL04  EXT  ID.NO  LOCATION CA  37251 37252 37254 37255 37256 37257 37258 37259 37260 37261 37262 37263 37264 37265 37266 37267 37268 37269 37270 37271 37272 37273 37274 37275 37276 37277 37278 37279 37280 37281 37282  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CU  191 . 9 6 2 1009 . 174* 395 . 44 1 8 9 9 . 0 8 3 * 0 .0 0 .0 180 . 4 4 4 899 . 0 8 3 * 383 . 9 2 3 1229 . 3 5 7 * 176 . 6 0 5 588 . 9 9 1 191 . 9 6 2 788 . 9 9 1 0 .0 0 .0 161 . 2 4 8 614 . 6 7 9 245 .711 348 6 2 4 245 711 647 706 3 2 6 . 335 460. 550 365 . 824 54 1 401 281 107 295 798 408 . 183 9 5 0 140* 489 . 049 340. 616 569 . 916 914 . 2 8 6 * 4 6 9 . 795 1 0 3 9 . 7 7 6 * 558 . 364 394 . 398 492 . 9 0 0 932 . 2 1 3 * 261 . 853 7 5 2 . 94 1 0. 0 0. 0 238 . 749 6 9 9 . 160 6 0 8 . 424 367 . 507 4 4 6 . 691 68 1 .232 3 6 5 . 824 591 . 597 4 7 3 . 646 555 742 496 . 751 5 5 9 . 328 577 . 617 785. 210 5 6 9 . 9 16 932 . 2 1 3 * 427 . 437 684 . 8 1 8  FE 1.766 1 .581 0 .0 1.930 2 . 300 2 .608 2 . 7 10 0 .0 2 . 7 10 2 .669 2 382 3 .121 2 320 2 793 2 105 2 . 148 2 .578 2 320 3 050 2 105 1 847 0 0 1 504 1 .547 1 . 1 17 1 .9 7 6 1 .504 2 .0 6 2 1 .762 1 .9 5 5 1 .3 1 0  LOCATION  MO 137 6 f 5 151 . 376 0 .0 91 743 68 . 8 0 7 82 . 5 6 9 45 . 8 7 2 0 0 321 101 77 . 982 45 872 4 5 . 872 2 8 . 88 1 24 0 6 7 601 6 8 5 72 . 202 57 . 762 1 10. 7 1 0 312 . 876 72 . 202 173. 285 0. 0 288 . 809 57 . 762 7 7 0 . 157 86 . 6 4 3 96 . 2 7 0 144 . 404 33 . 694 134 . 777 144 . 404  37251 37252 37254 37255 37256 37257 37258 37259 37260 3726 1 37262 37263 37264 37265 37266 37267 37268 37269 37270 37271 37272 37273 37274 37275 37276 37277 37278 37279 37280 3728 1 37282  EXT  0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 o 0 0 0 0 0 0 0 0 0 0 0 0  CA  3 5 . 996 2 5 . 197 0. 0 62 . 9 9 2 2 19. 5 7 3 5 0 . 394 5 9 . 393 0. 0 26 9 9 7 4 1 395 21 . 597 26 9 9 7 20 4 8 9 27 . 9 3 9 24 . 2 14 208 . 6 1 5 5 4 0 . 163 447 . 0 3 2 335 . 274 245 . 8 6 8 234 . 6 9 2 0 0 22 352 424 6 8 0 2 6 0 . 768 204 . 8 9 0 288 . 708 335 . 274 299 . 8 8 4 311 . 0 6 0 139 . 6 9 7  CU 3 0 . 323 41 . 0 2 6 0. 0 34 783 32 9 9 9 19 62 1 24 972 0 0 19 62 1 1 1 594 21 405 14 2 7 0 14 . 2 7 0 8 .027 24 . 0 8 0 26 . 756 23 . 188 24 . 9 7 2 8 .027 24 . 9 7 2 29 . 4 3 1 0 .0 15 . 162 8 027 16 054 378 13 1 1 . 594 1 1 594 18 . 7 2 9 2 1. 4 0 5 15 . 162  FE 0 121 0 . 133 0. 0 0 . 140 0 . 120 0 120 0 . 140 0. 0 0 140 0 . 123 0 134 0 150 0 148 0 . 191 0 132 0 125 0 167 0 . 155 0 . 143 0 . 1 19 0 . 1 19 0 .0 0 089 0 095 0 062 0 0 I2 0 . 078 0 .13 1 0 . 109 0 .098 0 .089  MO 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 28 0 7 0 0. 0 0 0 0 Q— 0 0 0 .0 20 0 5 0 0 .0 0 .0 0 .0 15 . 0 3 8 0 .0 0 .0 0 .0 0 .0 0 0 45 1 13 0 .0 0 0 0 .0 0 .0 0 .0 0 .0  NH40X 10%  HCL  ID.NO ID.NO  CA CU  FE  o  0  0  0  828  50. 505  0. 3 1 5  0  0  0  1. 2 7 6  24. 335  0. 2 4 2  0. 0  37285  0  0  0  510  365. 0 1 9  0. 7 5 2  37286  356  1804. 8 1 6 *  0. 6 1 0  0. 0  0. 6 5 4  0  0  0  1  37287  0  0  1 .563  37288  0  0  1 .467  37291 37292  0 0 0 0  75. 0 3 2  2 5 ., 0 6 3  o  J  J284  0  0  37285  O  0  37286  0  37287  0  o  6 .0 19 . 3 8 2  37288  0  0  0. 5 1 2  0 ,0  37289  0  0  19 . 3 8 2  0. 6 1 0  0 .,0  37290  0  0  23  370  0  0. 0  37291  0  0  0  0  37292  0  56. 781  0. 6 3 6  0 .0  37293  o  O  0. 4 6 8  O  0  6 8 .948  0. 5 7 1  0 .0  64. 892  0. 3 1 6  0  0  180  466  0  0 .877  172  0  1 .914  70. 9 7 6  0  1  786  37293  0  0  37294  0  0  1 .085  40  440  o. 4 0 3 o. 2 9 0  MO  0 .0  c  12 . 0 9 8  0 .038  0  9 0 .737  0 . 112  0 .0  193 .573 26 .213 8 .066  0 .055  0 .0  0  187  0 .0  0  080  0 .0  5 0 . 4 10  0 .131  0  0  259  32  0  078  0  0  0  16 . 131  0 .038  0  0  23  259  12 . 0 9 8  0  048  0  0  19  382  16  0 .053  0 .0  0 .063  0  262  131  37294  O  0  19 . 3 9 2  0  37295  0  0  23  37296  0  0  19  382  24 . 197  O .059  0  37297  0  0  0  0  30 . 246  O  029  0  0  0  O  20  164  0  067  0 .0  19  382  26  213'  0  37295  0  0  37296  0  0  1 .276  40. 558  0  1 .356  70. 9 7 6  0. 2 3 3  37298  O  64  o  0  892  0. 5 0 5  0  0  37299  89  0  558  FE  0 .0  1 .308  0  0  0 .0 27 . 135  413  60. 837  1  1 .914  37297  CU  MO  37283 37284  37290  LOCATION  LOCATION CA  37289  EXT  EXT.  0  259  8 .066 2 0 . 164  0  057  0  0 .0 0 .0 0  37298  0  0  1 . 164  0  0  069  0 .0  37299  0  0  1  227  0. 5 1 2  0  3730O  0  0  0. 0  12 .098  0 .027  0 .0  52. 725  0. 2 9 4  0 ,0  37301'  O  0  O  O  26  2 13  0  70. 9 7 6 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.3 0 0  0. 122  0. 0  0  0  35. 126  83. 624  0. 0 4 9  0. 0  3731 1  0  0  4 2 . 151  61 . 324  0. 0 3 1  0. 0  37312  0  0  52. 689  59. 466  0. 0 4 7  0 . 0_  KCL03 ID.NO  HN03:HCL04  EXT.  LOCATION  ID.NO CA  37284 37285 37286 37287 37288 37289 37290 37291 37292 37293 37294 37295 37296 37297 37298 37299 37300 37301 37302 37303 37304 37305 37306 37307 37308 37309 373.10 37311 37312  0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o 0 0 0 0 0 0 0 0 0  o 0  194 . 6 4 7 109 . 0 0 2 202 . 4 3 3 291 .971 2 14 . 1 12 155 7 18 128 467 272 . 5 0 6 303 . 6 5 0 256 934 15 t 8 2 5 2 14 . 1 1 2 327 . 0 0 7 179 . 0 7 5 155 . 7 1 8 163 . 5 0 4 186 .861 1 16 . 7 8 8 155 718 155. 718 236 724 464 . 9 9 3 287 4 5 0 380. 449 3 8 0 . 449 321 268 338 177 549 .538 845 .443  CU 371 .041 725 792 1628 . 9 5 8 * 479 638 5 1 0 407 633 .484 691 403 742 . 0 8 2 6 2 9 864 904 9 7 8 * 94 1 . 177* 642 534 1 176 4 7 1 * 923 .077* 707 692 792 7 6 0 597 285 1303 167* 1447 . 9 6 4 * 94 1 . 177* 1 2 8 8 . 837 745 6 8 5 * 579. 977* 1288 837 6 7 2 0 . 367 957 422 1509 .781 2209 .435 1583 4 2 9  FE 1 .406 2 .088 3 . 121 1 695 1 .509 1 .302 1 054 1 . 488 1 . 364 1 240 0 992 1 633 1 57 1 0 992 1 364 1 282 1 034 0 992 1 447 1. 5 3 0 0. 900* 1. 514 0. 922* 0. 592* 0 .867* 0 933* 1. 558 1 360 1 .360  LOCATION  MO 68 874 0 0 4? . 384 0 0 0 0 79 470 6 3 . 576 42 .384 105 . 9 6 0 84 768 169 536 2 1 1 . 92 1 1 16 556 52 9 8 0 68 874 2 6 . 490 0. 0 26 4 9 0 6 3 . 576 6 3 . 576 372 . 828 75 . 829 6 3 . 191 157 . 978 88 . 468 101 . 106 2 9 0 . 679 202 . 212 7 5 . 829  37284 37285 37286 37287 37288 37289 37290 37291 37292 37293 37294 37295 37296 37297 37298 37299 37300 37301 37302 ^303 37304 37305 37306 37307 37308 37309 37310 37311 37312  EXT.  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0  o 0 0 0 0 0  o 0  o o 0 0  o  0 0 0 0 0  o 0  o  0 0 0 0 0 0  CA  CU  48 . 7 4 9 2'2 6 3 3 20. 892 20 8 9 2 20 892 34 8 2 0 22 6 3 3 22 6 3 3 22 .. 6 3 3 24 . 374 15. 6 6 9 26 1 15 15 6 6 9 22 6 3 3 13. 9 2 8 17 4 10 13 9 2 8 10 4 4 6 13 9 2 8 15. 6 6 9 9 . 101 9 . 101 10. 9 2 2 10. 9 2 2 18. 202 10. 9 2 2 9 . 101 14. 562 18. 202  15 . 3 7 6 25 . 3 2 5 49 . 746 17 . 185 17 . 185 27 . 134. ' 2 1 . 707 22 . 6 1 2 18 . 9 9 4 33 4 6 5 27 . 134 26 2 3 0 33 . 4 6 5 26 2 3 0 19 . 8 9 8 . 2 1 . 707 18 . 0 8 9 21 . 707 25 325 2 5 . 325 30 . 839 10 . 8 8 4 7 256 31 746 10 . 8 8 4 16 327 28 . 1 18 42. 630 23. 583  FE 0 178 0 195 0 '214 0 131 0 131 0 . 195 0 . 132 0 . 1 12 0 . 125 0 . 172 0 162 0 . 265 0 . 190 0 . 160 0 . 202 0 . 226 0 . 1 19 0 . 1 12 0 . 131 o. 155 0 . 098 0 . 153 0 . 120 0 . 089 0 . 074 0 . 077 0 . 072 0 . 088 0 . 061  MO 0 0 0 .0 0 .0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 .0 0 0 0 0 0 0 0 0 0 0 0. 0 0 0 0 0 1 130 0 .0 0 0 0 0 0. 0 0. 0 0. 0 1. 507 0. 0  105. HCL ID.NO  EXT.  KCL03  LOCATION CA  37313 37314 37315 37316 37317 37318 37319 37320 37321 37322 37323 37324 37325 37326 37327 37328 37329 37330 37331 37332  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  NH40X ID . NO  37313 37314 37315 37316 37317 37318 37319 37320 37321 37322 37323 37324 37325 37326 37327 37328 37329 37330 37331 37332  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CU  110 . 8 5 5 2 .959 7 . 0 0 7 * 109 0 0 7 64 . 6 6 5 7 .786* 86 . 8 3 6 3 .036 84 . 9 8 8 1 .012 90 .531 3 .426 184 . 7 5 8 1 .090 97 . 9 2 1 3 .504 96 . 0 7 4 1 .869 59 . 122 1 .588 64 . 6 6 5 2 .211 25 . 335 2 .354 31 . 181 3 .948 58 . 4 6 5 4 . 100 7 0 . 158 2 .809 42 . 8 7 5 3 .492 9 . 1 10* 52 . 6 1 9 3 . 7 2 0 1 169 . 3 0 6 * 56 . 5 1 6 2 .885 52 . 6 1 9 O .683  'FE 0 .401 0 .566 1 .874* 0 .316 0 . 174 0 .288 0 . 174 0 .305 0 .261 0 .218 0 .475 0 .313 0 .280 0 . 157 0 . 179 0 .291 0 .302 0 .461 0 . 134 0 . 168  MO 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0  o.o 0.0 0.0 0.0 0.0 0.0 OQ  EXT  LOCATION CA  37314 37315 373)6 37317 37318 3 7 3 19 37320 37321 37322 37323 37324 37325 37326 37327 37328 37329 37330 37331 37332  .  O 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  HNO 3 : H C L 0 4  LOCATION  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  ID.NO  EXT.  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CA  CU  45 . 6 6 4 17 . 5 6 3 17 . 5 6 3 17 . 5 6 3 17 . 5 6 3 17 . 5 6 3 24 . 5 8 8 21 . 0 7 6 21 . 0 7 6 24 . 588 2 8 . . 101 25 . 0 0 0 35 .714 35 .714 32 143 2 8 . 571 3 5 . 714 21 . 4 2 9 7 143 17 . 8 5 7  • 2 9 . 733 5 5 . 749 3 . 717 96 . 632 6 5 . 041 52 . 0 3 3 6 5 . 041 42 . 74 1 48 . 316 2 9 . 733 2 0 . 441 2 0 . 633 15. 0 0 6 3 3 . 763 45. 018 18. 757 2 2 . 509 131 . 301 35. 639 3 0 . 012  FE 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0.  093 049 272 443 033 044 027 033 013 009 031 034 022 018 022 034 027 074 025 060  MO 0.0 0 0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0  o.o 0.0 0.0 0.0 0.0 0.0  o.o o.o  I D . NO  37313 37314 37315 373 16 37317 37318 37319 37320 37321 37322 37323 37324 37325 37326 37327 37328 37329 37330 37331 37332  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CU  7 2 7 . 0 8 1 2 0 6 2 139 1986 . 7 9 0 1583 . 4 2 9 5 9 1 8 . 0 9 8 * 8 2 8 539 1733 . 157 1 196 . 777 4 0 5 813 8 8 3 774 846 .950 1 3 1 0 . 436 2 5 3 6 3 3 1491 368 8 2 8 539 7 6 0 . 898 6 0 8 719 1067 894 346 . 631 423 . 475* 355 . 086 846 . 950 567 .488 558 290* 406 701* 591 . 133 647 0 2 5 * 709 .359 4 0 9 . 8 5 2 1 146 158 924 322 6 3 0 .542 1694 5 8 0 6 8 0 . 301* 591 . 133 2 1 2 5 . 9 3 9 4 3 3 . 498 1386 482 157 . 6 3 5 1 146 158  FE 2 .084 1 448 0 .922 O 98 7 0 . 592* 1 .382 1 .0 0 9 0 . 987 0 . 69 1 * 0 . 42 1 * 0 . 549* 0 478* 0. 698* 0. 889* 1 .338 1 .314 0 746* 1 .362 0 . 800* 0 . 848*  MO 6 3 191 31 596 56 872 183 254 75 829 101 106 2 4 0 . 127 164 . 297 189 . 574 82 . 149 101 . 106 324 0 0 6 188 . 513 117. 8 2 0 206 . 186 153 166 117 8 2 0 223 . 859 265 0 9 6 206 186  EXT.  LOCATION CU  CA O 0 0 O 0 0 0 0 0 0 0 0 0 O O 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0  o  0 0 0 0 0  o 0 0 0  18 . 2 0 2 131 . 0 5 8 136 . 5 1 9 72 . 8 1 0 23 . 6 6 3 21 . 8 4 3 10 . 9 2 2 12 . 7 4 2 18 . 2 0 2 9 . 101 9 . 101 138 . 7 2 8 64 . 7 4 0 162 . 7 7 5 162 . 7 7 5 277 . 4 5 7 231' . 2 1 4 577 . 1 10 532 . 7 1 7 455 . 0 2 9  32 44 27 45 31 36 45 25 30 9 21 53 77 44 32 44 44 30 67 25  .653 .444 .211 .351 . 746 .281 .351 .397 .839 .070 .769 .622 .838 .973 .865 .973 .973 .270 .459 . 946  FE .074 . 101 . 127 .057 .098 .077 .057 .060 . 104 .077 o .083 0 .251 0 . 205 0 . 160 0 . 165 0 .223 0 148 0 . 194 0 .340 0 . 285 0 0 0 0 0 0 0 0 0 0  MO 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .6 O .0 0 .0 0 .0 0 .0 27 . 4 3 5 32 . 9 2 2 4 1 . 152 0 .0 0 .0 0 .0 O .0 134 .431 21 . 9 4 8  10% HCL 10.NO  EXT.  NH40X. EXT  LOCATION CA  37333 37334 37335 37336 37337 37338 37339 37340 37341 37342 37343 37344 37345 37346 37347 37348 37349 37350 37351 37352 37353 37354 37355 37356 37357 37358 37359 37360 37361 37362 37363 37364 37365 37366 37367 37368 37370 37371 37372 37373 37374 37375 37376 37377 37378 37379 37380  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 O  o 0  o 0 0 0 0 0 0 0 0 0  o o o 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 . 342* 0. 258* 1. 0 6 3 1 093 0 . 987 1. 442 0 . 941 4 . 403 6 377 2 .505 1 291 1 .630 2 .963 0 .963 0 830 0 919 o .741 1 481 2 .444 2 .963 3 259 3 .481 2 .074 1 778 2 667 2 889 1 852 2 .370 1 .852 2 .400 2 .074 2 .252 3 . 185 3 .037 2 .326 2 .400 2 .370 2 874 2 .874 2 .400 2 .074 1 956 2 741 2 667 4 .889 3 .630 3 .437  CU 196. 8 3 3 146. 163 142. 266 136 . 4 1 9 54 . 568 74 . 0 5 6 247 . 5 0 3 95 493 64 312 165 6 5 2 93 .544 119 .231 76 . 9 2 3 6 9 .231 63 .462 150 . 0 0 0 117 . 3 0 8 5 0 OOO 126 . 9 2 3 46 . 154 61 . 5 3 8 67 . 3 0 8 61 . 5 3 8 92 308 119 .231 161 538 65 .385 80 .769 176 . 9 2 3 34 . 6 1 5 82 . 6 9 2 32 . 4 2 0 110 . 6 0 8 28 . 6 0 5 28 . 6 0 5 76 .281 43 . 8 6 2 83 . 9 0 9 143 . 0 2 7 64 . 8 3 9 78 188 61 0 2 5 57 .211 70 .560 80 .095 97 . 2 5 9 78 . 188  FE 0 . 398 0 . 224 0 . 492 0 . 380 0 . 407 0 . 260 0 . 380 0 . 425 0 . 215 0. 470 0 . 374 0 342 0 502 0 338 0 301 0 . 484 0 . 484 0 342 0 425 0 . ,301 0 406 0 . 388 0 445 0 553 0 . 411 0 285 0 . 516 0 548 0 . 457 0 .447 0 .511 0 421 0 374 0 . 333 o. 351 0 .437 0 225 0 495 0 ,423 0 401 0 . 464 0 . 428 o. 282 o. 315 0 439 0 374 0 . 523  MO 0 .0 0 0 0 .0 0 .0 0 ,0 0 ,0 0 0 0 0 0 .0 0 .0 0 .0 0 ,o 0 .0 0 .0 0 .0 0 .0 O .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 ,, 0 0 0 0 .0 0 .0 0 .0 0 .0 0 .0 0 0 0 0 0 0 0 0 0 0 0 0 0 <2.  ID.NO  LOCATION CA  37333 37334 37335 37336 37337 37338 37339 37340 3734 1 37342 37343 37344 37345 37346 37347 37348 37349 37350 37351 37352 37353 37354 37355 37356 37357 37358 37359 37360 37361 37362 37363 37364 37365 37366 37367 37368 37370 37371 37372 37373 37374 37375 37376 37377 37378 37379 37380  0 0 O 0 0 0 0 0 0 O 0 0 0 0 O 0 0 0 0 O 0 0 0 O 0 0 0 0  o o 0  o 0 0  o  0 0 0 0  o 0 0 0 0 0  o 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  14 . 2 8 6 10. 714 14 . 2 8 6 17 . 8 5 7 17 . 8 5 7 21 . 4 2 9 2 5 . OOO 2 5 . OOO 21 . 4 2 9 3 5 . 714 3 5 . 714 7 .236 io .854 18 0 8 9 18 . 0 8 9 21 . 7 0 7 21 . 7 0 7 21 . 7 0 7 28 . 9 4 3 10 . 8 5 4 18 . 0 8 9 14 . 4 7 1 43 .414 28 . 9 4 3 21 . 7 0 7 21 . 7 0 7 32 . 5 6 1 32 . 561 28 . 9 4 3 28 . 9 4 3 28 . 9 4 3 21 5 2 5 17 . 9 3 7 21 . 5 2 5 25 . 112 21 . 5 2 5 17 . 9 3 7 7 . 175 14 . 3 5 0 17 . 9 3 7 17 . 9 3 7 10 . 7 6 2 7 . 175 10 . 7 6 2 14 . 3 5 0 7 . 175 14 . 3 5 0  CU 58 148 9 3 . 787 39. 390 3 3 . 763 7 .503 24 . 385 48 . 7 6 9 16 . 882 2 0 . 633 3 0 . 012 18 . 757 79 . 6 3 0 20 . 370 68 . 5 1 9 27 . 7 7 8 44 . 4 4 4 40 .741 22 . 222 55 . 5 5 6 50 .000 61 . 1 1 1 53 . 7 0 4 22 . 222 59 . 259 40 .741 96 . 296 48 . 148 77 . 778 107 . 4 0 7 37 . 0 3 7 40 .741 36 . 2 8 1 217 . 6 8 7 18 . 1 4 1 29 .025 90 .703 32 . 6 5 3 68 . 9 3 4 9 0 . 703 36 . 281 47 . 166 50 .794 88 . 8 8 9 43 . 5 3 7 52 . 6 0 8 154 . 195 29 .025  FE 0 . 492 0 . 101 0 . 398 0 . 197 0 . 492 0 . 156 0 . 291 0 . 324 0 . 056 0 . 402 0 . 436 0 . 160 0 . 129 0 389 0 347 0 . 445 0 549 0 . 340 O .412 0 . 249 0 .214 O . 329 0 .434 O . 523 0 . 222 0 .093 0 . 289 0 267 0 . 345 0 423 0 . 467 1 . 170* 0 .675 0 . 169 0 .463 o .832 0 .202 0 .558 0 .457 0 .855 1 .417* 1 . 125* o .547 0 . 553 0 .697 0 .346 o .877  MO 0. 0 0 .,0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0 .0 0 .0 0 .0 0 .0 0 0 0 o 0 .0 0 .0 O .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .o 0 .0 0 .0 0 .0 0 .0 o .0 o .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 0 0 r\ 0 o 0 .0 o .0  • vy  KCL03 ID.NO  EXT.  HN03:HCL04  LOCATION CA  37333 37334 37335 37336 37337 37338 37339 37340 3734 1 37342 37343 37344 37345 37346 37347 37348 37349 37350 37351 37352 37353 37354 37355 37356 37357 37358 37359 37360 3736 1 37362 37363 37364 37365 37366 37367 37368 37370 37371 37372 37373 37374 37375 37376 37377 37378 37379 37380  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o 0 0  CU  882 . 759 1 109. 185 78 8 1 8 1 7 5 6 . 211 488 . 6 7 0 1 7 0 0 . 751 3 1 5 . 271 2 4 0 3 236 961 . 294 866 . 995 181 . 281 1441 . 94 1 1 5 7 6 . 355 2 6 2 5 0 7 3 1 3 0 0 . 493 2 0 7 0 4 8 0 9 8 5 . 222 1996 534 1497 537 3 6 2 3 341 827 586 1220 . 104 734 366 1892 857 624 .211 2321 . 4 2 9 881 239 1517 . 8 5 6 587 493 1 107 . 142 1468 732 1517 . 8 5 6 1211 .704 2 4 1 0 . 7 1 4 2 3 4 9 971 982 . 143 624 .211 2 6 0 7 . 143 1028 113 12 14 . 286 1468 732 1750 . 0 0 0 2 4 9 6 .844 2 0 5 3 572 6021 8 0 1 * 1392 857 2 9 3 7 463 232 1 . 4 2 9 1072 175 2 9 4 6 . 4 2 9 1432 014 4 2 8 5 715 2 4 2 3 407 15 17 . 8 5 6 2 7 1 7 154 2 0 0 0 . 0 0 0 2 2 7 6 535 4732 .14 1 2 6 4 3 718 982 . 143 1395 296 2053 . 572 1 312 1 166 . 8 5 0 0 .445 3093 .923 0 .474 1096 . 132 1 166 1 166 . 8 5 0 0 . 4 2 3 2 0 3 3 . 150 0 .394 1591 . 160 0 133* 1803 . 3 1 5 0 . 5 4 7 2828 . 729 0 . 2 1 9 * 1 149 . 171 0 452 1679 . 5 5 9 0 . 4 3 7 1166 . 8 5 0 0 . 197*1626 . 5 1 9 0 . 164*'1025 . 4 14 0 .270*1520 .442 0 .062* 3889 .503 0 . 186* 1591 . 160  FE  MO  3 632 7 0 . 692 1 .553 164. 948 4 . 1 10 176. 730 • 4 .182 141 384 2 987 2 3 5 . 64 1 88 . 365 2 509 4 062 164 948 4 .922 777 .614 2 939 235 .641 106 . 0 3 8 5 . 137 2 581 29 . 4 5 5 5 .043 371 . 6 1 3 3 .305 320 .000 3 .798 598 . 7 0 9 144 . 5 1 6 2 .897 6 . 223 77 . 4 1 9 5 .536 77 . 4 19 25 . 8 0 6 3 .433 5 258 216 .77,4 4 .506 41 . 290 4 . 185 185 . 8 0 6 4 .571 578 . 0 6 4 4 .077 25 . 8 0 6 6 .223 129 . 0 3 2 4 .292 51 . 6 1 3 4 .828 1 13 . 5 4 8 92 . 9 0 3 3 .326 3 433 25 . 8 0 6 5 .365 103 . 2 2 6 387 .097 2 . 747 4 .936 36 . 129 3 .322 142 . 6 7 5 4 .053 713 . 3 7 6 193 .631 3 367 2 1 4 .. 0 1 3 3 .012 407 . 6 4 3 2 .879 2 .702 1 12 . 102 3 .544 10 . 191 3 .322 50 .955 896 . 8 1 5 2 .658 71 . 338 3 .212 2 .769 433 . 121 2 . 9 9 0 2038 . 2 1 7 188 . 5 3 5 2 .481 3 . 101 591 . 0 8 3 4 .828 315 .924 107 . 0 0 6 2 .348  ID.NO  EXT.  LOCATION CA  37333 37334 37335 37336 37337 37338 37339 37340 37341 37342 37343 3/344 37345 37346 37347 37348 37349 37350 37351 37352 37353 37354 37355 37356 37357 37358 37359 37360 37361 37362 37363 37364 37365 37366 37367 37368 37370 37371 37372 37373 37374 37375 37376 37377 37378 37379 37380  0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 O O 0 0 0 0 0 0 0  o o o 0  o o 0 0 0  o 0 0 0  o 0  o 0  o o  0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0' 0 0 0  o 0 0  o  0 0 0 0 0 0 0  8 1 3 . 872 3421 966* 2996. 532* 2589. 596* 1072. 833* 1442. 775* 1 9 7 9 . 191* 2700. 579* 3052 . 024* 1572 . 2 5 4 * 2034 . 683* 33 . 9 6 2 41 . 5 0 9 39 . 6 2 3 28 . 302 3 0 . 189 56 . 6 0 4 33 . 9 6 2 28 . 3 0 2 22 . 6 4 2 254 . 7 1 7 18 . 8 6 8 56 . 6 0 4 77 . 3 5 8 192 . 4 5 3 22 . 6 4 2 211 . 3 2 1 160 3 7 7 28 302 233 .962 128 . 3 0 2 5416 .570 1536 . 6 1 5 1421 . 3 6 9 2919 .570 1382 . 9 5 5 998 . 8 0 0 1114 . 0 4 6 1 6 9 0 . 277 1440 577 4533 016 3226. 893 1094 8 3 8 1382. 955 1344 . 5 3 9 188. 235* 1575. 032  CU 39 . 7 8 4 41 514 38 0 5 4 4 5 . 838 6 9 . 189 82 . 162 3 9 . 784 6 0 . 541 131 . 4 5 9 2 5 . 081 47 . 5 6 8 19 . 6 2 6 13 . 0 8 4 15 . 8 8 8 29 . 9 0 7 19 . 6 2 6 16 . 8 2 2 56 . 0 7 5 32 . 7 1 0 26 . 168 20 .561 38 . 3 1 8 37 . 3 8 3 54 . 2 0 6 23 . 3 6 4 42 . 0 5 6 67 . 2 9 0 46 , 7 2 9 48 598 61 , 6 8 2 32 . 7 1 0 30 .022 79 . 4 7 0 30 . 9 0 5 24 . 7 2 4 54 . 7 4 6 39 . 7 3 5 37 . 0 8 6 70 . 6 4 0 30 022 39 735 28 256 30 905 33 . 5 5 4 42 384 88 3 0 0 35. 320  FE 0. 0. 0. 0. 0. 0. 0.  283 399 371 319 274 319 274 o. 376 1. 140* 0 . 257 0 . 388 0 .062 0 . 102 0 .077 0 .095 0 086 0 .071 0 079 0 . 101 0 . 125 0 .208 0 . 130 0 .249 0 .349 o .282 0 246 0 296 0 183 0 239 0 . 234 0 189 0 .260 0 .351 0 .294 0 .204 0 . 195 0 . 306 0 . 283 0 .238 0 .204 0 272 0 249 0 . 215 0 . 249 0 . 257 0 . 176 0 . 195  MO 9 8 . 765 3 7 3 . 114 0. 0 2 7 . 435 2 7 . 435 41 . 1S2 21 . 9 4 8 21 . 9 4 8 3 0 . 178 9 6 . 022 0. 0 O .0 0 .0 0 .0 18 . 6 1 7 0 .0 O .0 29 . 2 5 5 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 31 9 1 5 0 0 0. 0 0. 0 0 .0 65 .327 90 .452 0 .0 27 . 6 3 8 0 .0 0 .0 0 .0 27 6 3 8 0 0 3 0 . 151 1 2 5 . 628 15. 0 7 5 2 5 . 126 0. 0 0. 0  10% HCL ID.NO  EXT  NH40X  LOCATION CA  37381 37382 37383 37384 37385 37386 37387 37388 37389 37390 37391 37392 37393 37394 37395 37396 37397 37398 37399 37400 37401 37402 37403 37404 37405 37406 37407 37408 37409 3 7 4 10 374 1 1 3 7 4 12 3 7 4 13 3 7 4 14 3 7 4 15 3 7 4 16 3 7 4 17 3 7 4 18 37419 37420 3742 1 37422 37423 37424 37425  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 G  CU  0 . 3 6 3 *2212 . 157* 0 .267* 690 .346 0 . 2 9 9 * 533 .969 0 . 2 4 4 * 524 .434 0 . 2 9 6 * 722 .949 3 .536 136 . 9 8 0 1 .328 79 . 9 0 5 0 .952 209 .275 125 . 5 6 5 0 .649 1 .818 121 . 7 6 0 1 .876 163 . 6 1 5 4 .257 76 . 100 5 .051 5 5 . 172 1 .039 123 . 6 6 2 0 .981 194 . 0 5 5 0 . 5 3 4 * 144 . 5 9 0 2 .814 106 . 5 4 0 1 . 761 93 .222 1.905 161 . 7 1 2 1 .587 60 .880 2 193 19 . 0 2 5 2 .309 28 . 537 1 .660 3 6 . 147 2 .424 57 . 0 7 5 1 .991 58 .022 2 276 38 . 6 8 1 1 451 26 .374 1 792 40 .440 2 219 2 8 . 132 1 764 52 . 747 2 .. 2 7 6 43. 956 3 6 .. 9 2 3 2 133 2 901 24 . 6 1 5 3 .. 2 0 0 38 681 2 .. 7 3 1 4 2 . 198 5 6 . 264 2 873 2 . 076 29. 890 2 . 489 3 8 .. 6 8 1 2 , 176 36. 923 2 . 204 3 5 . 165 2 . 133 4 2 . 198 2 . 219 3 5 . 165 2 . 4 18 3 5 . 165 2 . 702 31 . 648 2 , 702 2 8 . 132  FE 0 532 0. 450 0 541 0..459 0 .436 0 .504 0 .411 0 .438 0 411 0 222 0 389 0..307 0 311 0 .. 3 6 2 0 .. 4 4 0 0 458 0. 289 0 311 0 167 0. 140 0 . 160 0 . 151 0 . 138 0 . 173 0 . 180 0 . 138 0 . 123 0 . 153 0 . 148 0 . 155 0 . 144 0 . 138 0 . 182 0 . 155 0 . 1 10 0 . 138 0 . 131 0 . 170 0 . 127 0 . 144 0 . 148 0 . 153 0 . 159 0 . 180 0 . 182  MO 641 .22 244 .27 2 1 9 .. 8 4 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0. 0 0. 0 0. 0 0..0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0  ID.NO  37381 37382 37383 37384 37385 37386 37387 37388 37389 37390 37391 37392 37393 37394 37395 37396 37397 37398 37399 37400 37401 37402 37403 37404 37405 37406 37407 37408 37409 37410 3741 1 3 7 4 12 37413 37414 37415 3 7 4 16 3 7 4 17 3 7 4 18 37419 37420 37421 37422 37423 37424 37425  EXT  LOCATION  0 0 0 O 0 0 0 O 0 O 0 0 0 0 0 0 O 0 O 0 0 0  o 0  o o 0 0  o 0  o o 0 0 0 0  o o  o  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o o o  o  o 0 0 0 0 0 0 0 0 0 0 0 0 0  o 0 0  0 0  o o 0 0 0  CA  CU  17. 937 17. 937 21 . 525 17 . 9 3 7 22. 912 22. 912 22. 912 22 9 1 2 19 0 9 3 15. 274 7. 637 3. 819 7. 637 15. 274 19. 0 9 3 19. 0 9 3 2 6 .. 7 3 0 1 1 . .4 5 6 7 637 15 2 7 4 1 1. 4 5 6 19 0 9 3 22 . 9 1 2 7 .637 27 . 9 6 5 19 . 9 7 5 19 . 9 7 5 19 . 9 7 5 19 . 9 7 5 23 . 9 7 0 19 . 9 7 5 19 . 9 7 5 0 .0 23 . 9 7 0 0 .0 27 . 9 6 5 19 . 9 7 5 23 . 9 7 0 19 . 9 7 5 19 . 9 7 5 0 .0 19 . 9 7 5 19 . 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0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0  KCL03 ID.NO  3 A  HN03:HCL04  LOCATION CA  37381 37382 37383 37384 37385 37386 37387 37388 37389 37390 3739 1 37392 37393 37394 37395 37396 37397 37398 37399 37400 37401 37402 37403 37404 37-105 37406 37407 37408 37409 374 10 374 1 1 374 12 374 13 37414 37415 37416 374 17 37418 374 19 37420 3742 1 37422 37423 37424 37425  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  6  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CU  0 . 0 0 7 * 654 . 144* o.0 2 0 * 1 1 3 1 . 491 0 . 0 1 6 * 1 5 5 5 . 801 0. 026*2864. 089 0 027 2 5 3 6 . 807 0 . 0 5 5 . 3 9 8 6 . 411 0 . 0 S 2 1721 . 4 0 5 0 . 0 4 9 7 0 6 6 . 816 0 0 2 8 2627 . 407 0 023 3 4 4 2 . 8 0 9 0 . 031 3442 . 809 0 0 9 8 1956 964 0 129 1630 804 0 1 13 2862 967 0 176 1812 0 0 5 0 . 0 7 0 1594 564 0 094 2 5 0 0 566 0 . 0 7 8 1902 6 0 5 0 . 0 3 9 3624 . 0 1 0 996 603 0 .022 684 . 9 3 8 * 0 076 474 745* 0 .055 761 . 0 4 2 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LOCATION CA  37381 37382 37383 37384 37385 37386 37387 37388 37389 37390 37391 37392 37393 37394 37395 37396 37397 37398 37399 37400 37401 37402 37403 37404 37405 37406 37407 37408 37409 37410 3741 1 37412 37413 37414 37415 37416 37417 37418 37419 37420 37421 37422 37423 37424 37425  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o 0 0  o 0 0 0 0 0 0 0 0 0  0 0 0  o 0  o 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  o o  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 • 0 0 0 0  9 .604* 195 . 9 1 9 * 1 19 . 0 8 8 * 201 . 6 8 1 * 171 . 6 0 3 39 OOI 204 . 7 5 3 224 .254 187 . 2 0 3 19 . 5 0 0 33 . 151 198 . 9 0 3 585 . 0 0 9 2262 . 0 3 5 * 2223 035* 347 . 105 146 . 2 5 2 54 . 6 0 1 27 . 3 0 0 9 .750 23 . 4 0 0 21 . 4 5 0 31 2 0 0 37 0 5 1 28. 402 30 .296 22 7 2 2 11 . 3 6 1 28 4 0 2 20 828 22 722 32 189 41 6 5 7 47 . 3 3 7 26 . 5 0 9 32 . 189 18 9 3 5 28 . 4 0 2 43 . 5 5 0 68 . 166 53 018 6 0 . 592 2 8 . 402 54 911 22 7 2 2  CU 31 . 7 8 8 36 . 2 0 3 35 . 320 64 . 4 5 9 56 . 6 7 1 89 .728 51 . 0 0 3 138 . 8 4 3 51 . 9 4 8 58 . 5 6 0 96 . 3 4 0 61 . 3 9 3 42 . 5 0 3 75 .561 54 782 73 672 56 671 39 . 6 6 9 81 . 2 2 8 35 . 8 9 1 18 . 8 9 0 1 1. 3 3 4 17 . 0 0 1 24 . 5 5 7 32 . 8 4 5 24 3 9 9 22 . 5 2 2 19 . 7 0 7 14 . 0 7 6 18 . 7 6 8 33 7 8 3 46 9 2 1 28 . 152 24 . 3 9 9 30 .968 38 . 4 7 5 13 . 138 29 . 0 9 1 28 . 152 28 . 152 29 0 9 1 2 2 . 522 23 . 4 6 0 23 4 6 0 24 3 9 9  FE 0 .066 0 .088 0 091 0 179 0 . 117 0 . 149 0 . 161 0 149 0 155 0 .083 0 199 0 219 0 201 0 . 183 0 . 149 0 . 177 0 . 155 0 138 0 . 108 0 .061 0 050 o 029 0. 035 0. 039 0 091 0 . 123 0 . 163 0 . 141 0 . 129 0 . 144 0 . 137 o. 152 0 . 118 0 102 0 129 0 . 107 0. 043 0. 093 0. 096 o.0 8 6 0 . 121 0 . 103 0 . 095 o. 101 0 . 151  MO 25 . 126 15 . 0 7 5 0 .0 22 . 6 1 3 35 .971 0 .0 23 .981 0 .0 0 .0 19 . 185 0 .0 38 . 3 6 9 14 . 3 8 8 0 .0 0 .0 0 .0 23 981 0 .0 45 .564 35 .971 28 . 7 7 7 23 .981 52 . 7 5 8 23 .981 260 .062 148 . 6 0 7 191 . 9 5 0 315 . 7 8 9 250 .774 210 .526 145 .511 278 . 6 3 8 95 .975 92 . 8 7 9 9 9 .071 92 . 8 7 9 46 . 4 4 0 49 .536 86 . 6 8 7 154 . 7 9 9 123. 8 3 9 92. 879 2 6 6 . 254 222 . 9 1 0 24 7 6 8  EXTRACTION-10%HCL  ID.NO  LOCATION CA  37426 37427 37428 37429 37430 37431 37432 37433 37434 37435 37436 37437 37438 37439 37440 37441 37442 37443 37444 37445 37446 37447 37448 37449 37450 37451 37452 37453 37454 37455 37456 37457 37458 37459 37460 37461 37462 37463 37464 37465  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  2 .642 0 .833 0 .801 1 . 121 1 .569 1 . 153 1 .249 1 .025 1 249 1 44 1 1. 201 1 249 0 833 1. 0 5 7 1..921 1 .057 1.. 6 6 5 1. 681 2 . 161 1..761 2 . 763 2 .633 3 .576 3 .283 3 .088 3 . 348 3 .088 2 .796 2 .568 3 .446 2. . 763 3 .446 2 .796 2 .958 2 .633 2 .211 2 .064 2 .536 2 .519 2 .048  CU 4 6 .. 5 3 2 5 3 . 691 71 . 5 8 8 102.. 0 1 3 75 . 168 76 . 9 5 8 60 .850 143 . 177 62 6 4 0 3 5 . .794 44 . 743 8 5 . 906 9 3 . 065 1 0 0 . 224 112. 752 53 691 1 9 3 . 289 1 16. 331 164. 653 1 2 8 ., 8 5 9 248 848 140 . 0 9 2 162 . 2 1 2 129 0 3 2 193 . 5 4 8 175. 115 1 10. 599 149, 309 132 719 165 . 8 9 9 160, . 3 6 9 141 936 1 19,. 8 1 6 193 548 1 19 816 165 . 8 9 9 160 369 152 . 9 9 5 248 . 8 4 8 377 . 8 8 0  FE 0 . 165 0 . 317 0. 475 0 . 697 0 . 349 0 , 296 0 . 232 0 . 321 0,.220 0 . 220 0 . 211 0. 260 0 . 203 0 . 296 0 . 423 0 . 232 0 . 423 0. 613 0 . 338 0 . 401 0 . 577 0 432 0 . 491 0 . 577 0 ..502 0 . 504 0 . 438 0 470 0 . 417 0 . 423 0 . 618 0 . 598 0 . 374 0 . 395 0 . 310 0 . 306 o. 331 o. 363 0 . 353 0 . 395  MC 0 .0 0 .0 0 0 0 ,. 0 0, . 0 0 0 0 .0 0 0 0 0 0 0 0 0 0 0 0, 0 0 0 0, 0 0,.0 0. 0 0. 0 0 0 0. 0 0 0 ,. 0 0 .0 0,. 0 0 .0 0 0 0. 0 0, 0 0. 0 0. 0 0 .0 0 .. 0 0 .0 0 .. 0 0 0 0. 0 0, 0 0 .0 0,.0 0. 0  .6  ID.NO  37466 37467 37468 37469 37470 37471 37472 37473 37474 37475 37476 37477 37478 37479 37480 37481 37482 37483 37484 37485 37486 37487 37488 37489 37490 37494 37495 37496 37497 37498 37499 37500 39101 39102 39103 39104 39105 39106 39107  LOCATION  0 0 0 0 O 0 0 O 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 O 0 0  o 0 0 0 0 0 0 0 0 0  o 0 0  o o o 0 0  o  0 0 0 0  o 0 0 0 0  o 0  o 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CA 2. 3 5 8 2 440 2 521 2 440 1 870 1 .952 1 269 1 529 2 . 375 1 757 2 684 1 139 2 033 2 . 440 2 765 2 .732 2 .960 1 .822 2 . 732 2 .472 1 .666 2 .810 2 . 304 1 797 1 666 2 ., 5 4 9 2 . 304 1 . 748 2 .222 2 .614 2 .418 2 94 1 2 . 745 3 30O 2 .320 2 .647 2 .402 1 .797 2 . 124  CU 157. 4 6 3 8 0 . 481 73, 483 7 5 . 232 101 . 4 7 6 87 . 4 8 0 157 4 6 3 94 . 4 7 8 87 . 4 8 0 108 4 7 5 2 0 9 . 951 87 . 4 8 0 197 704 194., 2 0 5 118 . 9 7 2 1 18 . 9 7 2 78 . 7 3 2 115 . 4 7 3 206 .452 136 . 4 6 8 126 . 8 7 2 186 . 7 8 4 183 . 2 6 0 197 . 3 5 7 81 . 0 5 7 96 . 9 1 6 114 537 112 7 7 5 1 19 8 2 4 74. 009 74 0 0 9 149 . 7 8 0 91 6 3 0 98 6 7 8 91 . 6 3 0 89 .868 84 582 79 . 2 9 5 52 8 6 3  FE  '  0 . 387 0 . 345 0 . 206 0 . 248 0 . 248 0 . 184 0 . 201 0 . 166 0 . 190 0 . 199 0 310 0 150 0 .254 0 265 0 .299 0 .442 O 365 0 .305 0 .343 0 .217 1 .346 2 .485 2 406 2 . 105 2 . 169 3. 245 2 20O 1 .4 5 6 0. 887 1. 2 0 3 1 741 2. 754 1 931 2 .090 1 377 1 409 1, 4 0 9 1. 2 3 5 0 . 887  MO 0. 0 0. o 0. 0 0. 0 0. 0  0 0  O. 0 0. 0 0. 0 O. 0 0. 0 0 0 0 0 0 0 0 .0 0 .0 0 0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 ,0 0 .0 0 .0 0 .0 0, 0 0 0 0 0 0 0 0 0 0 .0 0 .0 0 .0 0 0 0 0  EXTRACT 1 0 N - N H 4 0 X ID.NO  LOCATION CA  37427 37428 37429 37430 37431 37432 37433 37434  37435 37436 37437  37438 37439 37440 3744 1 37442 37443 37444 37445 37446 37447 37448 37449 37450 37451 37452 37453 37454 37455 37456 37457 37458 37459 37460 37461 37462 37463 37464 37465  0 0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  22 . 776 26 . 572 26. 572 18 . 9 8 0 3 0 . 368 18. 9 8 0 22 . 776 30. 368 26 . 572 22 . 776 3 4 . 164 26 . 572 22 . 776 22 . 7 7 6 3 0 . 368 30. 368 26 . 572 22 . 776 22. 776 4 5 . 525 37 . 9 3 7 3 4 . 143 64 493 56. 906 37 9 3 7 45 .525 18 . 9 6 9 18 . 9 6 9 22 . 762 30 .350 26 . 5 5 6 26 . 5 5 6 22 .762 26 . 5 5 6 22 . 7 6 2 30 .350 30 .350 22 . 7 6 2 26 .556  CU  3 5 . 359 51 . 271 56 . 575 44 . 199 35. 359 26. 519 91 . 934 35. 359 35. 359 24 . 7 5 1 6 5 . 414 54 . 807 72 . 4 8 6 79. 558 2 8 . 287 144 . 9 7 2 2 8 . 287 205. 083 120. 221 95 . 965 130. 861 9 0 . 731 62 .814 164 0 1 3 139 , 5 8 6 75 .027 106 . 4 3 4 83 . 751 73 . 282 59 . 324 59 . 324 61 .069 139 . 5 8 6 183 . 2 0 6 157 . 0 3 4 139 . 5 8 6 122 . 137 235 .551 584 .515  FE  0. 026 0. 044 0. 072 0. 044 0. 026 0. 022 0. 055 0. 031 0. 035 0. 028 0. 026 0. 01 1 0. 018 0 . 144 0. 022 0 . 144 0. 515 0 . 131 0 . 158 0 . 867 0 . 199 0. 481 0 .330 0 , 150 0 . 117 0 .226 0 .303 0 . 359 0 . 167 0 .665 0 .493 0 .255 0 . 171 0 .063 0 . 240 0 . 199 0 .238 0 . 142 0 . 188  MO  0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. o 0. o 0. 0 0. 0 0 0 0 0 0 .0 0 .0 0 .0 0 .0 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O 0. 0 19. 741. 23. 689 23. 689 23. 689 0. 0 19. 741 19. 741 19. 741 19. 741  113 . 4 1 3 66 . 303 55 . 8 3 4 52 . 345 80 .262 69 .793 235 .551 90 .731 83 .751 113 . 4 1 3 270 .447 139 . 5 8 6 184 . 9 5 1 314 .068 73 . 282 95 .965 43 .621 109 . 9 2 4 122 137 122 137 9 2 ., 6 5 0 138. 976 1 4 6 . 102 258. 352 6 4 . 143 74 . 8 3 3 1 15.813 71 . 269 8 0 . 178 26. 726 71 . 269 8 0 . 178 71 . 269 106. 904 121 . 158 112. 249 1 10.468 3 9 . 198 62 . 361  FE  0 .231 0 .282 0 .064 0 .043 0 . 171 0 .032 0 .021 0 .017 0 .032 0 .034 0 . 128 0 .026 0 .085 0 . 192 0 .068 0 . 137 0 .096 0 .075 0 .243 0 .049 0 .039 0 .240 0 459 0 138 0..232 o. 7 6 5 0 . 162 0. 055 0. 013 0. 011 0. 055 0 . 328 0. 066 0 . 087 0. 022 0. 026 0. 031 o. 0 1 7 0. 011  MO  0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 o 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 0 o 0,.0 0, 0 . 0.0 0. 0 0. 0 0. o 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0  EXTRACTI0N-KCL03 ID.NO  LOCATION CA  37427 37428 37429 37430 37431 37432 37433 37434 37435 37436 37437 37438 37439 37440 3744 1 37442 37443 37444 37445 37446 37447 37448 37449 37450 37451 37452 37453 37454 37455 37456 37457 37458 37459 37460 3746 1 37462 37463 37464 37465  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CU  291 . 572 0. 0 298 861 0 .. 0 4 3 7 . 358 0 .. 0 379 .043 0 0 204 100 0 .0 218 6 7 9 0 .. 0 174 . 9 4 3 0 .0 335 . 307 0 .0 687 6 0 4 * 328 . 0 1 8 364 4 6 5 .0 . 0 437 . 358 0 .0 652 .342* 145.. 786 218 . 6 7 9 0 .0 7289 297* 0 .0 204 . 100 O 0 5466 .969* 0 .0 0 .0 1501 . 594 1625 . 5 1 3 0 .0 743 . 5 0 8 0 .0 7 5 9 . . 193 O o 1 3 6 6 .. 548 0 .. 0 1594 .. 306 0 0 3 0 3 6 . 772 0 0 7 7 4 3 .. 7 7 0 * 0 0 1518 . 386 0 0 2201 . 6 6 0 0. 0 6 8 3 . . 274 0 0 7 5 9 . 193 0 0 7 5 9 . 193 0 .. 0 1328 588 0 0 1078.. 0 5 5 0 0 797 . 153 0. 0 6 8 3 . 274 0. 0 873 .072 0. 0 4 9 3 . . 476 0 .. 0 531 . 435 0 0 7 8 9 . 561 0 0 531 . 4 3 5 0 0 531 .. 4 3 5 0. 0  FE  1 .612 2 .407 1 .397 1 . 333 1 .376 0 .559* 1 .397 0 .688* 4 .621 1 .397 1 .548 1 .720 2 . 192 4 .084 1 . 720 4 . 191 3 .439 4 .836 4 .084 4 .565 3 .304 3 .913 2 .500 4 . 130 2 . 565 2 283 3 696 3 .OOO 2 .065 3 . 152 2 935 3 .913 2 .500 3 522 4 . 348 2 261 3. 152 3 522 5. 652  MO  331 .034 4 6 8 . 965 8 8 2 . 759 1655 172 811 0 3 4 336 552 1544 . 8 2 7 744 . 8 2 7 182 . 0 6 9 562 . 759 8 0 0 OOO 242 . 7 5 9 369 . 6 5 5 165 . 5 1 7 248 276 110 . 3 4 5 93 . 7 9 3 154 . 4 8 3 160 OOO 2 1 0 526 548 348 558 , 140 151 . 7 7 5 425 9 4 9 1468 788 7 1 9 . 706 205. 630 146. 8 7 9 181 . 151 73. 439 78 335 122. 399 6 8 0 . 539 328 0 2 9 2 6 9 . 278 342 . 717 127. 295 181 . 151 156. 671  ID.NO  LOCATION CA  37466 37467 37468 37469 37470 37471 37472 37473 37474 37475 37476 37477 37478 37479 37480 37481 37482 37483 37484 37485 37486 37487 37488 37489 37490 37494 37495 37496 37497 37498 37499 37500 39101 39102 39103 39104 39105 39106 39107  0 0 0 0 0 O 0 O 0 0 0 O O 0 0 0 0 O O 0 0 0 0 0 0 0 0  o  0 0 0 0 0 0  o 0  o o 0  593 967 0 0 2635 .730 7 0 5 .. 3 3 6 0 816 705 0 787 . 0 0 7 0 4 1 5 777 0 423 .202 0 482 598 0 0 1789 3 2 6 608 817 0 0 6 6 0 . 789 6 5 3 .. 3 6 4 0 430. 626 0 0 8 9 0 . 951 0 1113 6 8 9 0 8 9 0 9 .. 5 1 2 * 0 2301 . 6 2 4 5 3 4 ..571 0 4 4 5 .. 4 7 5 0 504 . 872 0 o 999 .534 0 492 . 3 0 8 0 775 .757 313 287 0 o 432 .634 0 1976 . 6 8 9 0 760 .839 5 2 2 . 144 0 447 .552 0 462 .471 0 0 5967 . 363* 0 6862 .469* 0 3058 .275 0 1603 . 7 2 9 6 8 6 . 247 0 0 1230 . 7 7 0 0 2871 . 7 9 4 537 . 0 6 3 0 686 .247 0  CU  0. 0 0. 0 0 0 0 0 0 0 0 0 0 0 0 o 0 0 0 .0 0 0 0. 0 0 0 0 0 0 0 0. 0 o 0 o 0 0 0 0. 0 0 0 . o .0 0 .0 0 .0 0 .0 0 0 0 .0 0 .0 0 .0 0 .0 o .0 0 0 0 .0 0 .0 o .0 0 .0 0 .0 0 .0 0 .0  FE  MO  3. 016 3 6 0 . 947 5 3 2 . 544 2. 4 0 4 1. 5 3 0 153. 846 1. 2 6 8 136. 0 9 5 857. 989 1. 6 3 9 1. 3 7 7 502. 959 4. 699 3 3 7 . 278 0 . 765* 532 544 1 093 183 4 3 2 284 024 2 404 307. 692 3 716 177 5 1 5 5 .355 3 . 0 1 6 1301 . 7 7 6 6 . 120 355 . 0 3 0 414 .201 3 .060 177 5 1 5 4 . 153 4 1 4 . 201 3. 169 183 . 4 3 2 3 .322 2 .754 147 . 9 2 9 473 .373 2 .295 413 .625 2 .050 107 . 0 5 6 3 .344 48 . 6 6 2 2 .805 3 .452 199 . 5 1 3 2 .265 180 . 0 4 9 2 .977 399 .027 194 . 6 4 7 1 .834 433 . 0 9 0 3 .020 389 .294 2 .503 1 .402 656 .934 3 .452 340 .632 3 .020 170 . 3 1 6 457 .421 3 .020 394 . 160 3 .366 3 .560 150 . 8 5 2 2 . 2 0 1 1002 . 4 3 3 1 . 9 4 2 1021 . 8 9 7 1 .942 175 . 182 486 .618 2 .546  EXTRACTI0N-KCL03  EXTRACTION-10WCL ID.NO  ID.NO  LOCATION CA  39109 391 10 391 1 1 3 9 1 12 3 9 1 13 3 9 1 14 3 9 1 15 3 9 1 1G 3 9 117 3 9 1 18 3 9 1 19 3 9 120 3 9 12 1 3 9 122 3 9 123 3 9 124 39125 3915 1 3 9 152 39153 3 9 154 39155 39156  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  2 .091 2 .944 2 .706 2 .854 2 .899 2 .706 0 0 0 .0 2 .602 2 .453 2 .007 1 .962 2 . 260 1 992 2 .810 2 . 304 0 966 2 .044 2 347 2 . 165 2 .574 2 .5 13  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  2 .301  CU  14 0 0 16 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 13 0 0 0  .097 .0 .0 .638 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 0 .0 .0 .0 .0 .212 .0 .0 .0  FE  4 670 0 .975* 1. 105* 1.040* 0 .997* 0 .997* 1 .040* 0 .0 0 .758 0 .715 0 607 0 633 0 . 769 0 726 0 997* 0 769 0 .271 0 881 0 .. 8 1 6 0 .709 0 806 0 . 799 0 692  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 O 0 0 0 0  .0  :o .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 0 .0 .0 .0 .0 .0 .0 .0 ,0 .0  •Pi  LOCATION  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  23. 689 52 574 35 .049 35 .049 35 .049 35 .049 2 1. 0 3 0 0 .0 24 . 5 3 5 24 . 5 3 5 21 24 21 24 28 24 35 20 17 17 17 17 17  .030 .535 .030 .535 .039 .535 .049 .938 .448 . 448 .448 . 448 . 448  3 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  563 .0 .0 .0 .0 .0 0 0 .0 0 .0 .0 0 .0 .0 .0 .0 .0 0 .0 0 .0 .0  MC  FE  CU  CA  3 9 109 3 9 1 10 39 1 1 1 3 9 1 12 3 9 1 13 3 9 1 14 3 9 1 15 3 9 1 16 3 9 1 17 3 9 1 18 3 9 1 19 39120 39121 39122 39123 39124 39125 3 9 15 1 39152 3 9 153 39154 39 155 39156  CA  39109 391 10 391 1 1 3 9 1 12 3 9 1 13 3 9 1 14 3 9 1 15 3 9 1 16 3 9 1 17 3 9 1 18 3 9 1 19 39120 39121 39122 39123 39124 39 125 39151 39152 39 153 39154 39155 39156  O O 0 0 0 0 0 O 0 0 O O 0 O O O O 0 O O O 0 O  0 0 0 0 0 0 0 0 0 0  5 3 7 .. 0 6 3 3 9 0 . 381 506 . 745 52 1 7 6 0 570. 557 487 . 977 450. 440 0. 0 431 . 6 7 2 465. 455 356 . 598 412. 903 401 . 6 4 2 315. 308 570. 557 431 . 6 7 2 9 3 8 . 4 17 305 471 4 17 2 2 9 2 8 3 .. 1 2 0 3 9 1 153 484 . 284 402 . 328  o 0 0 0 0 0  o 0 0  o  0 0  o  CU  MO  FE  164 . 7 6 0 * 58 974 53 846 123 . 0 7 7 128 2 0 5 8 9 744 66 . 667 0. 0 184 . 6 1 6 6 4 ., 1 0 3 5 1 .2 8 2 35. 897 4 6 . 154 64 . 103 189. 744 107 . 6 9 2 158 9 7 4 80 223 62 . 396 9 2 . 108 175. 302 2 9 7 . 122  0 . 194* 0. 702 0. 672 0. 566 0. 733 0. 794 0. 859 0. 0 1 .2 6 2 * 1 6. 2 8 * 1 .7 5 1 * 1 669* 1 .2 8 2 * 0. 696 0 662 0. 855 4 . 173' 0. 0 9 6 * 0 904* 0 171* 0 4 18* 0. 6 1 2 * 0. 337*  0. 0  9. 732 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0 0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0  EXTRACTION- -HCL04  EX T R A C T I O N - N H 4 0 X ID . NO  LOCATION  MO  0. 052 0 025 0 .. 0 3 8 0 031 0 034 0 03 1 0 020 0 0 0 .007 .0 0 0 9 002 0. 002 0. 016 0 020 0. 029 0 .013 0 179 0 035 0 035 0 042 0 .035 0 042 0 024  'o.  0 0 0 0 0 .0 0 0 0 0 0 0 0 .0 0 0 0 0 0 0 0 0 0 0 0 0 0 .0 0 0 0. 0 0 0 0 0 0 0 0 0 0 0 0 0. 0  o  I D . NO  LOCATION  39109 391 10 391 1 1 3 9 1 12 3 9 1 13 3 9 1 14 3 9 1 15 3 9 1 16 3 9 1 17 391 I B 391 19 39120 39121 39122 39123 39124 39125 39151 39152 39153 3 9 154 3 9 155 39156  O O 0 O 0 0 O 0 0 0 0 O 0 O 0  o o o 0  o 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  117. 3 1 5 26 . 0 4 7 27 .907 27 . 9 0 7 26 . 0 4 7 27 . 9 0 7 26 .047 0 .0 26 . 0 4 7 27 . 9 0 7 29 .767 29 . 767  0 0 0 0 0 0 0  1600 . 0 0 1 * 20 . 828 20 .828 1 1. 3 6 1 22 . 7 2 2 20 828 17 . 0 4 1  o  27 24 31 27  .907 . 186 .628 .907  11 0 0 0 0 0 O O O O 0 0 0 0 0 0 0 0 0 0 0 7 0  .2 1 5 .0 .0 .0 .0 .0 .0 .0 .0 .0 0  o  0 0 0 0 0 .0 .0 .0 .0 .888 0  M0_  FE  CU  CA  1  .  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  ,081  4  .060 .078 .045 .060 .059 .058  0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0 0 0.0 0.0 0.0  O .077 .079 .082 .089 .066 .076 .058 .060 432 .051 .080 .044 .045 .072 069  944  oo 0.0 0.0  o:o 0.0 0.0 0.0 0.0 0.0  EXTRACTION-  I D . N O  I D . NO  3 9 157 39158 39159 3 9 1GO 39 161 3 9 162 39163 ' 39164 3 9 165 3 9 166 39 167 39 168 39 169 39 1 7 0 39 1 7 1 39 172 39 173 39174 39 1 7 5 39 1 26 39127 3 9 128  I  EXTRACT  1 0 W C L  CA  0 0 0 0 0 0 0 0 0 0 0  0 0 0  0 0  o 0 0 0  0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 . 37 1 • 7 6 . 6 3 1 44 . 9 2 2 0 .939 18 . 4 9 7 0 .391* 0 .0 0 . 787 1 . 347 0 .0 0 .0 0 . 238* 0 .0 0 . 436* 2 . 6 19 0 .0 0 .0 0 . 8 18 18 . 4 9 7 1 . 226 26 . 424 1 .317 0 .0 0 .500' 47 . 5 6 4 1 . 135 1 .665 42 . 279 1.446 56 . 958 3 1 .068 0 .959 188 . 9 9 7 0 . 87 1 36 . 246 0 . 738 25 . 890 0 . 723 0 .0 1 . 1 15 0 .0 0 .877 0 . 2 3 0 * 3 16 . 1 1 8  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  . 230 .408 .378 .206 .269 . 157 .494 .520 322 . 247 . 206 . 125 . 200 .526 .422 . 359 . 333 .283 .425 . t47 . 329 .444  0 0 0 0 0 0 0 0 0 0 0 0 0 0  .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0  6  0 0 0 0 0 0 0  EXTRACTI0N-NH40X I D . NO  39159 39 160 3 9 1.6 1 39 162 3 9 163 3 9 164 39165 3 9 166 3 9 167 39168 39169 39170  0 0 0 0 0 0 0 0 0 0 0 0  39126 39127 3 9 128  0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0  39157 39158 39159 39160 39161 39162 39163 39164 39165 39166 3 9 167 39168 39 169 39 170 3917 1 3 9 172 3 9 173 39174 3 9 175 39126 39127 39128  ID.NO  CA  0 0  CA  CU  0 0 0 0 0 0 O O O 0 0 0 0 0 0 0 O 0 0 0 O 0  0 0 0 0 0 0 0  134 . 1 0 9 0 .0 0 O 137 . 8 3 5 253 318 44 . 7 0 3 7 0 .. 7 8 0 301 . 746 186 2 6 3 4 2 8 .. 4 0 5 186 . 2 6 3 9 3 132 149 . 0 1 0 7525 . 03 1 ' 3395 6 1 8 ' 1439 447 848 905 634 . 833 9 3 0 . 104 4G9 . 2 0 8 930 .910 93 . 8 4 2  172 3 3 1 O 0 O 0 80 . 223 8 6 165 1 15. 877 199. 072 124 7 9 1 175 . 3 0 2 148. 561 460. 539 1 18. 8 4 9 555 618 347 . 632 325 . 105' 268 . 6 8 2 ' 456 . 7 5 9 ' 166. 5 8 3 ' 158 . 5 2 2 ' 1 17 . 9 4 9 292 .308 64 1 . 0 2 6  o 0 0 0 0 0 0 0 0  o 0 0 0 0 0  FE  i  2 249 0 0 0. 0 3 . 213 5. 522 2 . 530 3 253 2 .851 0 .663* 3 213 1 . 124 4. 257 1 .3 2 5 5. 221 2 . 723 5. 817 5 . 054 4 . 229 5 . 364 2 .972' 5 . 394' 4 . 723*  MO  o;;o  0 0 0 0 0 0 0 0 O. 0 0. 0 O. 0 0. 0 0. 0 0. 0 32 . 0 0 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0. 0 0 .0 O .0 0  o  o  EXTRACTI0N-HCL04  LOCAIION  39 157 39 158  LOCATION  MO  FE  CU  ION-KCL03  24 . 4 2 7 0. 0 0. 0 2 0 . 938 2 0 . 938 27 . 9 1 7 24 . 4 2 7 20. 938 31 . 407 34 . 8 9 6 27 . 9 1 7 31 . 407 31 . 407 38 . 386  31 . 544 42 . 0 5 9 31 . 544  4 5 . 7 14 0 0 0. 0  0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 0. 0 18 . 8 2 4 0. 0  0. 0 0. 0 67 . 170  0 .0 5 9 0 0. 0. 0.  0 0 017 03 1 017 026 024 240 063 024 026 026 677  o. 0. 0. 0. 0 0 0 0. 0.  0. 018 0 . 150 0 . 222  LOCATION  MO  FE  CU  0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0. 0.  00 0 0 0 0 0 0 0 0 0 0 0 0  0. 0 0. 0 0 0  CA  3 9 157 39158 39159 39160 39161 39162 39163 39164 39165 39166 39167 39168. 39169 39170 39171 39172 39173 39174 39175 39126 39127 39128  0 O O O O O O 0 0 0 O 0 0 0 0 0 O 0  o  o 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  143 . 9 0 5 .0 0 O 15 . 1 4 8 13 . 2 5 4 17 . 0 4 1 0 O 9 .467 17 . 0 4 1 1 4 0 . 1 18 17 . 0 4 1 13 2 5 4 15 1 4 8 4525. 441* 3087 .060* 231 530 436. 706 681 . 412 5 6 0 . 94 1 446 .512 697 .675 26 .047  o  CU  7 . 888 0 .0 0 .0 0 .0 0 .0 0 .0 10 5 1 8 0 .0 0 0 13 . 1 4 7 35. 497 0. 0 512. 736* IO. 518 7 869 0. 0 1 3 . 1 15 O. 0 0. 0 0 .0 13 7 9 3 34 4 8 3  FE  0 . 234 0 .0 0 .0 0 . 144 0 . 296 0 165 O 181 0 . 154 0 .090 0 809* 0. 362 0. 306 4 . 468* 0. 441 0 . 364 0. 986* 1 .0 7 1 * 0. 707* 0 . 77 1 * 0. 283 0. 416 1 101*  MO  "0-0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0  o.o 0.0  o.o  0.0 0 0 0 0 0.0 0.0  E X T R A C T I O N - 107.HCL ID.NO  CA 39129 39130 3 9 131 39132 39133 39134 39135 3913G 3 9 137 39138 39 139 39140 3 9 14 1 3 9 142 39143 3 9 144 39145 3 9 14G 39147 3 9 148 39149  EXTRACT I O N - K C L O G  LOCATION  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 .966 0 .922 0 .666* 1.059 0 .817 2 . 148 1 .558 2 . 148 0 .908 0 .598* 2 .754 1 .437 2 . 148 1 . 725 1 .891 1.906 1.891 2 . 270 1 .574 1 .604 1 .997  CU 44 . 3 6 7 49 .913 123 : 2 8 3 179 . 5 6 4 9 9 . 163 69 .682 120 . 6 0 3 131 . 323 251 . 926 7 12 . 8 9 8 75 . 0 4 2 329 .648 3 5 9 . 129 101 . 8 4 3 58 .962 249 . 246 1 5 8 . 124 125 . 9 6 3 37 . 5 2 1 77 . 722 16 . 0 8 0  FE 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  .481 .466 .435 .594 .293 .568 . 403 . 747 .505 . 308 . 250 .439 .371 .36 1 .204 .286 .371 .206 . 280 . 288 .265  MO 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0  E X T R A C T I O N - NH40X I D NO  L O C A T I ON  0 0 0 0 0 0 0 0 0 O 0 0 0 0 0 0 0 0 0  o 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  LOCATION CA  39129 39130 39131 39132 39133 39134 39135 39136 39137 39138 39139 39140 39141 39142 39143 39144 39145 39146 39147 39148 39149  0 O 0 O 0 O 0 0 0 0 0 0 O 0 0 O 0 0 0 O O  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  157 . 6 5 4 259 003 91 . 272 251 . 911 149 6 8 6 474 . 615 332 . 231 1387 . 337 474 . 615 7 19 . 2 2 5 3 103 . 2 5 3 * 1223 . 04 7 4 6 3 . 6G3 3 3 9 . 532 3 3 9 . 532 1058 . 757 8 4 3 . 355 744 . 781 306 . 674 5 1 1 . 124 4 4 5 . 408  CU  FE  723 .077 7 12 . 8 2 1 320 . 256* 427 . 863* 458 607* 0 .0 O 0 0 0 484 . 228* 0 0 0. 0 0. 0 0. 0 ; 0. 0 0. 0 0. O 0. 0 O. 0 7 3 0 . 185* 0. 0 599. 520*  5 .. 0 8 9 * 4 . 926* 4 . 529 7 . 146 2 . 778 4 . 932 3 . 926 6 . 885 2 . 577 3. 865 5. 737 5. 939 5. 596 6 . 865 5. 435 6 . 442 7. 690 3. 946 6. 482 7 . 549 6 . 34 1  CU  FE  MO 0 0 0 0 4 8 OOO 4 8 OOO 32 0 0 0 1 1 2 . OOO 3 2 . OOO 8 0 . OOO 0. 0 0. 0 0. 0 48. 000 64 . 0 0 0 3 2 . OOO 96. 000 48 . 0 0 0 48 . 0 0 0 560. 000 128 . 0 0 0 64. 000 32 . 0 0 0  E X T R A C T I O N -• H C L 0 4  CA 39129 39 130 39131 3 9 132 39133 3 9 134 39135 3 9 13G 39137 3 9 138 39139 39140 3914 1 39142 39143 39144 39145 39146 39147 39148 39149  ID.NO  CU  31 . 544 0 .0 3 1 . 544 2 1 . 49'j 43 . 5 1 3 . 25 . 765 25 . 765 43 .513 39 . 887 2 8 . 34 1 33 . 494 39 . 887 43 . 5 1 3 51 . 530 4 7 . 139 25 . 765 2 5 7G5 43 . 5 1 3 1 10 . 7 8 9 25 . 382 18 . 1 3 0 25 . 765 5 4 10G 18 . 1 3 0 82 .448 2 1 . 756 2 1 . 756 30 .918 18 . 1 3 0 15 . 4 5 9 18 . 1 3 0 92 . 754 79 .87 1 21 . 756 21 . 756 33 . 494 2 1 .756 18 . 0 3 5 25 . 382 36 .07 1 . 0 0 8 29 12 . 8 8 2  MO  FE  0 101 0 1 12 0 .037  0 .074 0 .013 0 .059 0 048 0 . 144 0 . 129 0 .055 0 061 0 .083 0 . 129 0 . 122 0 .046 0 .096 0 . 1 16 0 .044 0 .074 0 .079 0 .072  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 .0 .0 .0 .0 .0 .0  o  .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0 .0  ID.NO  LOCATION CA  39129 39130 39131 39132 39133 39134 39135 39136 39137 39138 39.139 39140 3914 1 39142 39143 39144 39145 39146 39147 39148 39149  '  0 0 0 0 O O O O 0 O O O O 0 O 0  o 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  26 . 0 4 7 27 . 9 0 7 58 .381 82 .098 56 . 5 5 6 56 .556 65 .678 448 . B03 156 . 8 9 9 246 .294 1988 . 5 9 8 * 363 .056 85 . 747 94 . 8 6 9 45 . 6 1 0 363 .056 328 .392 1 2 0 . 4 10 7 1 . 152 162 3 7 2 83 .922  22 17 13 21 19 57 141 62 20 50 34 57 39 66 43 62 48 91 34 57 32  .069 . 93 1 .605 . 769 .048 . 143 .497 .585 .408 . 340 .014 . 143 .456 .667 .537 .585 .980 . 156 .014 . 143 .653  1 . 166* 1. 295* 0 .270 0 .303 0 .201 0 . 384 0 . 438 0 . 376 0 . 136 0 .214 0 . 254 0 .290 0 . 335 0 .305 0 .254 0 .255 0 . 294 0 . 222 0 . 303 0 . 344 0 .277  MO  0  .o  0 .0 0 .0 0 .0 .0 .0 0 .0 .0 .0 0 .0 0 .0 0 .0 0 .0 0 .0 .0 0 .0 0 .0 i 19 . 8 4 0 26 .631 0 .0 0 .0  o o o o  o  EXTRACTION-lOZHCL ID.NO  EXTRACT 1 0 N - K C L 0 3  LOCATION CA  39150 39176 39177 39178 39179 39180 3 9 18 1 39182 39183 39184 3 9 185 39 186 39187 39188 39189  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 O O 0 0 0 0 0 0 0 0 0 0 0  1 .3 7 7 1 .7 7 1 1 .697 1 .5 3 5 1 .3 2 8 2 . 730 1 .4 6 1 2 080 1 608 0. 989 1 874 2 .597 1 682 1 682 1 859  CU 184 9 2 5 188 9 9 7 9 0 . 6 15 1 19 . 0 9 4 1 2 6 .. 8 6 1 1 16 5 0 5 1 16 . 5 0 5 1 6 3 . 107 186 4 0 8 165 . 6 9 6 165 . 6 9 6 113 . 9 1 6 100 . 9 7 1 113 . 9 1 6 67 .314  FE 0. 0. 0. 0. 0. 0. 0. 0. 0. 0 0 0 0 0 0  445 601 353 364 279 690 263 335 366 274 364 468 364 229 512  MO 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0  o.o 0.0  EXTRACT 1 0 N - N H 4 0 X I D . NO  39150  0  0  32 . 6 3 5  LOCATION CA  39150 39 1 7 6 39177 39178 39179 39180 39181 39182 39183 39184 39185 39186 39187 39188 39189  0 0 0 0 O 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 O 0 O 0 0 0 0 0 0  o  CU  FE  0 .0 0 .0 0 .0 0 o 0 .0 0 o O .0 0 .0 0 o 0 o O o 0. o 0 0 0. 0 o.0  4 .066 4 .848 2 .950 3 .507 2 . 393 0 .0 2 .888 4 .229 5 013 2 599 4 . 229 1 877 1 .6 0 9 0 . 763» 0. 0  CA  CU  FE  67 5 0 3 154 . 3 5 3 2 0 5 . 177 472 47 1 152 47 1 O O 54 588 56 471 86 .588 3 0 . 118 239 059 120 4 7 1 26 353 22 5 8 8 0. 0  73 469 103 6 0 7 76 .066 123 . 2 7 9 86 557 0 O 8 9 . 180 112 7 8 7 1 19 . 3 4 4 94 426 81 312 62 951 41 . 967 57. 705 0. 0  303 .023 479 .815 4 2 8 . 143 564 . 706 369 .089 0 0 232 526 350 635 328 489 147 6 3 6 498 . 270 5 7 5 . 779 2 10. 3B1 2 7 3 . 126 O. O  MO 1 7 6 • OOO 204 . 724 236 .220 7B . 7 4 0 346 .457 O .0 1 to. 2 3 6 62 992 283 464 125 9 8 4 2 2 0 472 47 244 314 9 6 0 236 220 236 220  EXTRACT 1 0 N - H C L 0 4  LOCATION CA  ID.NO  CU 33  494  FE 0. 090  MO  o.o  ID.NO  39150 39176 39177 39178 39179 39180 39181 39182 39183 39184 39185 39186 39187 39188 39189  LOCATION  0 0 O 0 0 O 0 0 0 O 0 0 0 0 0  O O 0 0 0 0 O 0 0 0 0 0 0 0 0  0 236 1.071' 0 .803* 0 .857* 0 .771* 0 .0 0 .803» 0 .836* 1 007* 0 354 0 836* 0. 289 0. 094 0. 091 . 0 .0  MO 26 .631 237 .500 65 .625 62 .500 231 250 0 .0 146 8 7 5 37 . 5 0 0 221 875 37 5 0 0 143 7 5 0 0 0 350. 000 162 . 5 0 0 0. 0  EXTRACTION-10%HCL ID.NO  CA 3 9 19 1 3 9 192 3 9 193 39194 39 195 39 1 9 6 39 1 9 7  0 0 0 0 0 0  39200  0 0 0  30 198 nn 199 39?0 1 39202 39203 3920-1 39205  EXTRACT 1 0 N - K C L 0 3  LOCATION  0 0 0  0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  1 245 1. 306 1 44 1 2 . 551 1. 5 1 6 2 . 776 1 080 2 881 0 597* 1 . 44 1 0 780 1 .095 2 . 236 1 170 1 636  CU 29 5 3 0 2 1 .4 7 7 18 7 9 2 40. 268 24 161 0 0 0 0 24 161 26 8 4 6 0 0 18 7 9 2 37 . 5 8 4 18 . 7 9 2 26 . 8 4 6 42 . 9 5 3  FE 0 230 0. 525 0 477 0. 351 0 534 0. 306 0. 542 0. 258 0 223 0 310 0 156 0 .633 0 . 456 0 651 0 . 466  Mn  ID.NO  LOCATION CU  FE  MO  0. O 0. 0 O. 0 0. 0 0. 0 0. 0 0. 0 0 0 O 0 0 0 0 0 0 .0 0 .0 0 .0 0 0  -p-  OO  I  EXTRACTI0N-NH40X ID  NO  E X TRACT I O N - H C L 0 4  LOCATION CA  39191 39192 3 9 193 3 9 194 3 9 195 39196 3 9 197 3 9 198 3 9 199 39200 39201 39202 39203 39204 39205  0 0  0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  40 33 . 40 29 . 22 25 33 29. 33 33 33 . 48 . 37 . 51 . 48 .  835 4 11 835 698 274 986 4 1 1 698 4 1 1 4 11 4 1 1 260 123 972 260  CU  FE  MU  0 .0 0 .0  0 077 1 463* 0 936 0 077 0 355 o. 2 0 2 0 559 0 056 0 043 0. 247 0 022 0. 624 0 624 0 . 16 1 0. 592  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0  0  0 0 0 0  0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0  .0 .0 0 0 0 0 0 0 0 .0 .0 0 0 0 0  D.NO  39191 39192 39193 39194 39195 39196 39197 3 9 198 39199 3920O 39201 39202 39203 39204 39205  LOCATION  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  0 0 0 0 0 0 0 0 0 0 0 0 0 0 0  CA  CU  254 .417 5559 . 480* 8103 .645* 563 .486 582 .332 282 .685 4 2 4 0 . 28 1 • 124 3 8 2 94 2 2 9 2280 330* 75. 383 8480. 563* 1865. 7 2 3 * 5069 . 492* 9422. 848*  0 .0 0 .0 0 .0 16 . 0 5 4 0 O 0 .0 0 .0 13 . 3 7 8 0 .0 0 .0 0 O 9. 365 9 . 365 0. 0 0. O  FE 0 . 153 0 . 169 0 . 290 0 .771* 0 . 127 0 322 0.. 227 0. 348 0. 285 0 280 0 . 127 0. 792* 0 . 364 0 . 264 O 232  MO 0 .0 0 .0 O .0 0 .0 0 .0 0.. 0 0.. 0 0..0 0, o 0. o 0. 0 0. 0 0. 0 0. 0 O r>  

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