Relative ages of strata-form sulfide ore and wallrock determined by a structural analysis of the

Copper Queen Mine, Yavapai County, Arizona

Item Type text; Thesis-Reproduction (electronic); maps

Authors Brook, Doyle Kenneth, 1944-

Publisher The University of Arizona.

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RELATIVE AGES OF STRATA-FORM SULFIDE ORE AND WALL ROCK

DETERMINED BY A STRUCTURAL ANALYSIS OF THE

COPPER QUEEN M INE, YAVAPAI COUNTY, ARIZONA

by

D o y le Kenneth Brook, Jr.

A T h e sis Subm itted to the F acu lty o f the

DEPARTMENT OF GEOSCIENCES

In P artia l F u lfillm en t o f the R equirem ents For the D egree o f

MASTER OF SCIENCE

In the G raduate C o lle g e

THE UNIVERSITY OF ARIZONA

1 9 7 4

STATEMENT BY AUTHOR

This th e s is has been subm itted in p artia l fu lfillm ent of re ­quirem ents for an advanced degree at The U niversity of Arizona and is deposited in the U niversity Library to be made availab le to borrowers under ru les of the Library.

Brief quotations from th is th e s is are allow able w ithout sp ec ia l perm ission , provided that accu ra te acknowledgm ent of source is m ade. R equests for perm ission for ex tended quotation from or reproduction of th is m anuscript in whole or in part may be granted by the head of the major departm ent or the Dean of the G raduate C ollege when in h is judg­ment the proposed use of the m aterial is in the in te re s ts of scho lar­sh ip . In a ll o ther in s ta n c e s , how ever, perm ission must be obtained from the author.

SIGNED:

APPROVAL BY THESIS DIRECTOR

This theses has been approved on the date shown below:

>RGE H . DAVIS A ssis tan t Professor of G eo sc ien ces

// / f l /Date

DEDICATION

This t h e s is i s r e sp e c tfu lly d ed ica ted to

u n c le , th e la te Howard E. D a v is . H is g u id a n ce and

encouragem en t stron g ly in flu en ced my d e c is io n to

pursue g e o lo g y a s a c a reer .

i i i

ACKNOWLEDG MENTS

This p ro ject b egan as an exp loration program for C om inco Amer­

ic a n I n c . , and I w ould lik e to ack n ow led ge the co o p era tio n and a s s i s ­

ta n ce o f M r. Hugh M oore and M r. G ene France o f th e C om inco s ta f f .

D r. G eorge H . D a v is contribu ted s ig n if ic a n tly to th e s u c c e s s o f th is

t h e s is by h is in s is t e n c e on c le a r ly d efin ed g o a ls for th e in v e s t ig a t io n

and by h is untiring a s s is ta n c e during it s preparation . I w ould lik e to

thank D r s . Sp en cer R. T it le y , John M . G u ilb ert, and D onald E. L iv in g s­

ton for th eir h e lp fu l d is c u s s io n and r ev ie w s o f th is t h e s i s . S p e c ia l

thanks go to Tom H eid r ich , a fe llo w graduate s tu d en t, w h o se a s s is ta n c e

w ith the com puter program data w a s in v a lu a b le ; to M r. and M rs. Rex •

R ick s, operators o f the C opper Q ueen m in e, for th eir k in d n ess and h o s ­

p ita lity during my work in M ayer, Arizona; and to my fr ie n d s , Phil

A nderson and S p en cer Sm ith, for th eir com m ents and for a s s is t a n c e in

the f ie ld . A s p e c ia l word o f p ra ise i s g iv e n to my w ife , M aria, w h o se

p a tien ce and understanding made th is th e s is p o s s ib le .

iv

TABLE OF CONTENTS

LIST OF ILLUSTRATIONS............................................................. ..................................v i i

ABSTRACT......................................................................................................................... ix

INTR O D U C TIO N .................................................................................................................... 1

Purpose o f S tu d y .......................................................................................................... 2M e t h o d s ...................................................................................... 2L ocation and A c c e s s ............................................................................................... 4H istory and P revious W o r k .................................................................................. 6

GEOLOGIC SETTING. . ' .................................................................................................. 8

Rock U n it s .................................................................................................................. 8Spud M ountain V o l c a n i c s ........................................................ 8

R h y o lite -D a c ite M em b er ................................................................... 10M arker-bed M em ber............................................................................. 12

S u lfid e -r ic h B a n d s ...................................................................... 13Banded Iron F orm ation s................................................... 16

T u ff-B reccia M e m b e r ..................................................... 19Q uartz V e i n s ....................................................................................................... 21D ia b a se D i k e s ....................................................................................................21

Structural F e a t u r e s .................................................................................................. 22Sh ylock Fault Z o n e ....................................................................................... 22Hum boldt S y n c lin e ............................................................................................. 23F o l ia t io n ................................................................................................................. 23

F o lia tio n o f S u lfid e M in e r a ls ........................................................... 26B ed d in g .....................................................................................................................29F o l d s ........................................................................................................................ 32

F old s in S u lfid e -r ich B a n d s .............................................................. 34Fold M o rp h o lo g y ...................................................................................... 34F o ld -a x is O r ien ta tio n ............................................................................ 37

F a u lts ............................................................................. 37J o in t s ...................................................................................................... 39L in ea tio n ................................................................................................................. 40

PRECAMBRIAN HISTORY OF THE REGION ..................................................................41

D e p o s it io n o f the Y avapai S e r i e s ..................................................................... 41The M a za tza l R ev o lu tio n ..........................................................................................42The Grand C anyon D is tu r b a n ce ............................................................................42

Page

v

TABLE OF CONTENTS— C ontinued

GEOLOGIC HISTORY OF THE COPPER QUEEN MINE A R E A ............................ 43

D e p o s it io n o f the R h y o lite -D a c ite M e m b e r .................................................43D e p o s it io n o f th e M arker-bed M em b er ...........................................................43D e p o s it io n o f the T u ff-B reccia M e m b e r ........................................................46E ffects o f the F irst D e fo r m a tio n ........................................................................ 47E ffec ts o f the S econd D eform ation ..................................................................... 47K inem atic M odel for Structural H is to r y ...........................................................49

SULFIDE HISTORY............................................................................................................. 51

D eform ation o f the S u lfid e -r ich B a n d s ...........................................................51O rigin o f the S u lfid e M in e r a l iz a t io n .......................................................... 51

COMPARISON OF THE COPPER QUEEN ORE BODY WITHSIMILAR D E PO SIT S...................................................................................................... 55

Jerom e, A r iz o n a ...................................................................................................... 55N oranda, Q u e b e c .................................................................................................. 55

CO N C LU SIO N S...................................................... 57

vi

Page

REFERENCES 58

LIST OF ILLUSTRATIONS

1. G eo lo g ic map o f the C opper Q u een mine area ,Y avapai C ounty, A rizon a ..........................................................in p o ck et

2 . G e o lo g ic map o f the 300 and 400 l e v e l s , CopperQ ueen m in e, Y avapai C ounty , A r izo n a .............. ... in p o ck e t

3 . L ocation map. C opper Q ueen mine area ,Y avapai C ounty , A rizon a ....................................................................... 5

4 . G eo lo g y o f the M ayer area , Y avapai C ounty, A r iz o n a .............. 9

5 . Outcrop o f r h y o lite -d a c ite m e m b e r ....................................................... 11

6 . P o lish ed s la b o f sp ec im en from m arker-bed m e m b e r ................. 11

7 . S u lfid e -r ich bands in the m arker-bed m e m b e r ............................... 14

8 . T yp ica l su lfid e m ineral a sse m b la g e o f c h a lc o p y r ite ,p y r ite , a rsen o p y rite , and sp h a ler ite in s u lf id e -rich b a n d s .................................................................................... 15

9 . Pyrite gra in s from su lf id e -r ic h b a n d s ................................................... 17

10 . Outcrop o f banded iron f o r m a t io n .......................................................... 18

1 1 . O utcrops o f v o lc a n ic b recc ia o f th e tu ff-b r e c c ia member . . . 20

1 2 . Lower h em isp h ere p o le -d e n s ity diagram o f p o le sto bedding for the M ayer a r e a .............................................................. 24

13 . Lower h em isp h ere p o le -d e n s ity diagram o f a x e s o fminor fo ld s for the M ayer area . . . ................................................24

14 . Lower hem isphere p o le -d e n s ity diagram o f p o le s tofo lia tio n at the Copper Q ueen mine a r e a .......................................... 25

15 . Lower hem isphere p o le -d e n s ity diagram o f p o le s toa x ia l su rfa ces for a ll fo ld s m easured in theM ayer a r e a ....................................................................................................... 25

16 . Fold lim bs in sed im entary rocks cu t by tra n sp o sitio nalong a x ia l-p la n e f o l i a t i o n ..................................................................... 27

Figure Page

v ii

LIST OF ILLUSTRATIONS— C ontinued

Figure Page

17 . C lo s e ly sp a ced s lip su r fa ces w hich h av e a lm o st-formed r o o t le s s fo ld s in th in ly bedded sed im entaryr o c k ........................................................................................................................27

1 8 . Fragm ented zon ed pyrite grain w ith fragm entsex ten d ed p a r a lle l to fo l ia t io n ..................................................................28

1 9 . C h a lcop yrite lam inae concordant w ith fo lia t io n . .............................28

2 0 . P ressure shadow o f ch a lco p y r ite around zonedpyrite g r a i n .......................................................................................................30

2 1 . Lower hem isph ere p o le -d e n s ity diagram o f p o le s tobedding for the Copper Q ueen mine a r e a ......................................31

2 2 . M e so sc o p ic is o c l in a l fold with tigh t asym m etricp a r a s it ic fo ld s in the m arker-bed m em b er.......................................33

2 3 . K in k-fo lded fo lia tio n in the tu ff-b r e c c ia member,400 le v e l . C opper Q ueen m in e .............................................................. 35

2 4 . I s o c lin a l fo ld s in su lf id e -r ic h bands e x p o se d inr a ise b e tw een 400 and 300 l e v e l s , C opperQ ueen m i n e .......................................................................................................35

2 5 . H u d le sto n 's c la s s i f ic a t io n o f fold forms ................................................. 36

2 6 . C om p ila tion o f fo ld forms for C opper Q ueen m inearea , b a se d on H u d le sto n 's c l a s s i f i c a t i o n ................................... 36

2 7 . Lower h em isp h ere p ro jec tio n s o f fo ld a x e s .......................................... 38

2 8 . Fragm ent o f lam in ated su lf id e -r ic h band e x p o se don 400 l e v e l ....................................................................................................... 52

v iii

ABSTRACT

The C opper Q ueen m in e, near M ayer, A rizona, is a strata-form

cop p er su lfid e d e p o s it in Precam brian m eta v o lca n ic and m etased im en tary

rock s o f the Y avapai S e r ie s . The d e p o s it l i e s on th e e a ster n flank o f the

Hum boldt sy n c lin e and w ith in the S h ylock fau lt z o n e . At the C opper

Q ueen m in e, the e n c lo s in g Spud M ountain V o lca n ics are d iv id ed in to

three m em bers: the r h y o lite -d a c ite m em ber, the m arker-bed m em ber,

and the tu ff-b r e c c ia m em ber. C opper m in era liza tio n i s r e s tr ic ted to the

m arker-bed m em ber, w hich i s interpreted to be an e x h a l i t e . D e ta ile d

a n a ly s is o f the structural fabric o f su lf id e m in erals and e n c lo s in g w a ll

rock s p rov id es a m ethod for e s ta b lis h in g th eir deform ational h is to r y .

The stru ctu ra l fab rics o f the rock s and su lf id e m in erals are

s ta t is t ic a l ly h o m o g en eo u s . Fold m orphology o b serv ed in the bands o f

su lfid e m in erals are s ta t is t ic a l ly h o m o g en eo u s . Both the rock s and the

su lfid e m in erals h a v e undergone tw o p eriod s o f d eform ation . Tight to

i s o c l in a l fo ld s , a x ia l-p la n e fo lia t io n , and major rev erse fa u lts w ere

formed during th e fir st p er io d . Sm all fa u lts and d ia b a s ic in tru sio n s w ere

im p osed on the rock s during the sec o n d p er io d . The d e p o s it i s in ter ­

preted to be a sy n g e n e tic a ccu m u la tion o f su lfid e m in erals formed during

subm arine fum arolic a c t iv ity . The th ick s e q u e n c e s o f th e r h y o lite -d a c ite

member co u ld rep resen t the p y r o c la s t ic dom es d ev e lo p ed around fum a­

ro lic v e n t s .

ix

INTRODUCTION

The C opper Q ueen m in e, near M ayer, A rizona, i s a strata-form

copper su lfid e d e p o s it in Precam brian m eta v o lca n ic and m etased im en tary

r o c k s .o f the Y avapai S e r ie s . This C opper Q ueen mine i s not to be c o n ­

fu sed w ith th e C opper Q u een m ine near B agdad, A rizon a. The rock s th at

h o s t th e d e p o s it are is o c l in a l ly fo ld ed and h a v e b een m etam orphosed to

lo w -g ra d e g r e e n s c h is t f a c i e s . Fold ing and m etam orphism took p la c e

concurrently during a major Precam brian te c to n ic e v e n t .

The C opper Q u een m ine sh a res many g e o lo g ic fea tu res w ith

strata-form su lfid e d e p o s its that are thought to h a v e a s y n g e n e t ic , v o l -

c a n o g e n ic o r ig in . T h ese in c lu d e the a s s o c ia t io n o f the d e p o s it w ith a"

th ick seq u e n c e o f subm arine v o lc a n ic r o c k s , o ccu rren ce o f the su lfid e

m in era liza tio n a t a r h y o lite -a n d e s ite c o n ta c t , banded nature o f the ore

z o n e , la tera l gradation o f th e ore zon e in to un m in era lized bedded t u f f s ,

and th e conform able re la t io n sh ip b e tw e en su lf id e -r ic h bands and b ed ­

ding in the country rock . H o w ev er , to d a te , th e d e p o s it h a s b een in ter­

preted to be e p ig e n e t ic in o r ig in . S p e c if ic a l ly , Lindgren (1926) c la s s i f i e d

the C opper Q ueen ore body a s a Precam brian, p y r it ic , rep lacem en t ty p e .

E ven sen (1969) p rop osed th at the d evelop m en t o f th e C opper Q u een ore

body i s p o s t - fo l ia t io n and th at the ore zo n e w a s formed in stru ctu ra lly

favorab le z o n e s in the s c h is t . He further p rop osed that the cop p er s u l­

f id e s co u ld h ave b e e n sca v e n g e d from th e country rock by hydrotherm al

f lu id s . Both Lindgren and E ven sen reco g n ized the Precam brian age o f

1

the fo ld in g , and E ven sen s p e c if ic a l ly attributed the fo ld in g to the

M a za tza l R evo lu tion .

2

Purpose o f Study

In order to e v a lu a te w hether the C opper Q ueen ore body i s sy n -

g e n e t ic or e p ig e n e t ic , the age o f the su lf id e s r e la t iv e to the e n c lo s in g

w a ll rock m ust be d eterm in ed . The g o a ls o f th is in v e s t ig a t io n are th ree­

fold: (1) to determ ine the age o f th e s u lf id e s r e la t iv e to the te c to n ic

e v en t that fo ld ed th e rock s o f th e study area , (2) to determ ine the age

o f the s u lf id e s r e la t iv e to th e e n c lo s in g w a ll ro ck , and (3) to d ev e lo p a

m odel for the g e n e s is and deform ational h isto ry o f the d e p o s it .

M ethods

A strata-form su lfid e ore body occurring in fo ld ed rock s o ffers

a unique opportunity to determ ine the age o f the su lfid e m in era liza tio n

r e la tiv e to th e a g e o f d eform ation . A d e ta iled a n a ly s is o f the structural

fabric o f the su lfid e m in era liza tio n and the e n c lo s in g w a ll rock s p ro v id es

a m eans for e s ta b lis h in g th e deform ational h is to ry o f the su lf id e m in erals

and w a ll r o ck s , r e s p e c t iv e ly . A s t a t is t ic a l h om ogen eity o f structural

fabric o f both the su lfid e m inerals and th e w a ll rock w ould im ply th at

both h av e undergone the sam e h isto ry o f deform ation . If su ch s t a t is t ic a l

h om ogen eity e x is t s at th e C opper Q u een m in e, it w ould im ply th at the

su lf id e -r ic h b a n d s , w hich c o n s titu te the ore z o n e , w ere deform ed by th e

sam e fold ing ev en t that a ffec te d the e n c lo s in g r o c k s . H o w ev er , a pre­

deform ation age for th e su lf id e m in erals d o es not n e c e s s a r i ly im ply a

sy n g e n e tic o r ig in . The su lf id e -r ic h bands co u ld be the r e su lt o f e p i­

g e n e t ic rep lacem en t o f s e le c te d rock s prior to d eform ation . M inera l

3

texture that w ould s u g g e s t an e p ig e n e tic or ig in for the su lf id e s are (1)

rep lacem en t tex tu res b e tw een su lfid e and s i l ic a t e m in erals and (2) a

rec o g n iz a b le p a ra g en etic seq u e n c e o f su lf id e m in e r a ls . M ineral tex tu res

that w ould s u g g e s t a sy n g e n e tic or ig in for the su lf id e s are (1) su lf id e

m inerals sh ow in g primary growth zon in g and (2) fram boidal accu m u la ­

tio n s o f su lfid e g r a in s . If th e structural fab rics for the s u lf id e -r ic h

bands and w a ll rock w ere found to be in h om ogen eou s w ith r e sp e c t to

one another, th is w ould im ply th at th e su lf id e -r ic h bands and w a ll rock

h ave not undergone the sam e h isto ry o f deform ation and are c o n se q u e n tly

o f d ifferen t a g e s . If the su lfid e m in erals w ere "concentrated" (E ven sen ,

1969) after th e rock s w ere fo ld ed , there shou ld be no sim ila r ity b e tw een

th e fabrics' o f the su lf id e -r ic h bands and the w a ll rock a t th e C opper

Q ueen m in e.

Structural a n a ly s is o f the C opper Q u een rock s w a s done in tw o

s t a g e s . The fir st s ta g e in v o lv ed a d e scr ip t iv e and geom etric a n a ly s is o f

the m e so sc o p ic e lem en ts th at c o n stitu te the structural fa b r ic . The s e c ­

ond s ta g e attem pted through k in em atic a n a ly s is o f the d e sc r ip t iv e and

geom etric data to reco n stru ct th e m ovem ents that took p la c e w ith in th e

rock s during deform ation (Turner and W e is s , 1 9 6 3 ) . The k in em atic a n a l­

y s i s o f fo ld ed rock s h a s d ev e lo p ed from San der's (1930) c o n c ep t th at

the sym m etry o f th e structural fabric r e f le c ts th e sym m etry o f the m ove­

m ents that g en era ted th e fa b r ic .

O rien tation data for fabric e lem en ts w ere c o l le c te d during g e o ­

lo g ic mapping and recorded d ir e c tly on m a r k -se n se com puter c a r d s .

T h ese data w ere red u ced by com puter to low er h em isp h ere p o le -d e n s ity

d iagram s, w hich w ere contoured by h an d . R egion al fabric data w ere

4

ob ta in ed from e x is t in g g e o lo g ic quadrangle maps (Anderson and C r e a se y ,

1958; A nderson, 1972) and from two s e le c te d lo c a l i t ie s o u ts id e th e C op­

per Q ueen m ine area: Power Line G ulch and the B lu eb e ll m in e.

G e o lo g ic mapping w a s in it ia lly done on b la c k -a n d -w h ite a er ia l

photographs havin g a s c a le o f 1 :2 4 0 0 . D ata w ere th en transferred to a

1 :2400- s c a le topographic map ob ta in ed by en larg in g a portion o f the

M ayer 15-m inute quadrangle (F ig. 1, in p o c k e t ) . Underground g e o lo g ic

mapping w a s done on l : 2 4 0 - s c a le m ine m aps prepared by G ene France

o f C om inco Am erican I n c . and me (F ig . 2 , in p o c k e t ) .

Petrographic and m ineragraphic study o f the rock s perm itted

id e n tif ic a tio n o f the rock ty p es and su lfid e m in erals p resen t at th e C op­

per Q ueen m in e. Petrographic work a ls o a llo w ed the determ in ation o f

m etam orphic grade and d e ta ilin g o f the structural fabric on a m icro sco p ic

s c a le .

L ocation and A c c e ss

The C opper Q u een m ine l i e s approxim ately 6 m ile s n orth east o f

M ayer, A rizona, a sm a ll tow n lo c a te d on State H ighw ay 6 9 , som e 25

m iles so u th e a s t o f P resco tt (F ig . 3 ) . The reg ion h a s a m oderate r e l ie f

o f 300 to 500 fe e t and l i e s in W ilso n 's (1962) T ran sition Zone p h y s io ­

graphic p ro v in ce . W ilso n d e sc r ib e s the p rovin ce as b ein g more rugged

than the C olorado P lateau to the n orth east and lack in g the broad p e d i­

m ents b e tw een ran ges c h a r a c te r is t ic o f the B asin and Range p rov in ce to

the so u th w e s t . T y p ic a lly , the p rov in ce i s ch a ra cter ized by h i l l s and

m ountains sep ara ted by dry w a sh e s and in term itten t s tr ea m s. The m ine

p orta l, a t an e le v a t io n o f 4 ,3 0 0 f e e t , i s one m ile north o f the Agua Fria

5

Flagstaff

Prescott

HumboldtWilliamson

Copper # Queen / Mine

BellRanch

Flagstaff Phoenix 70 miles

Prescott Mayer

O Phoenix

5 miles

O Tucson

Figure 3 . L ocation m ap. C opper Q u een mine area , Y avapai C ounty, Arizona

6

River in s e c . 6 , T . 12 N . , R. 1 1 /2 E . , Y avapai C oun ty , A rizona. The

mine w orkings ex ten d northward into s e c . 3 6 , T. 13 IM. , R. 1 1 /2 E.

Two m ile s o f rough road co n n e c t the m ine area to a co u n ty -m a in ta in ed

g ravel road lead in g from the B ell Ranch to M ayer.

H isto ry and P revious Work

Num erous go ld m ining cam ps w ere a c tiv e in the Bradshaw M oun­

ta in s as early as th e 1 8 6 0 's . H ow ever, the su rface ex p o su res o f cop p er

o x id e on ly 8 m ile s e a s t o f the m ountains r e c e iv e d l it t le n o t ice u n til the

la te 1 8 9 0 's . L a r g e -sc a le m ining a c t iv ity did not b eg in at the C opper

Q ueen m ine u n til th e early 1 9 0 0 's . M ining p e r s is te d u n til 1 9 2 3 , w hen

the ex trem ely low p rice o f copper forced a ll o f the m in es in th e area to

c lo s e dow n . Production w a s lim ited to th e ore en cou n tered in d e v e lo p ­

m ent work and probably did not e x c e e d 7 5 ,0 0 0 ton s (D o u g la s , 1 9 5 6 ).

The e a r lie s t s ig n if ic a n t g e o lo g ic work in the area w a s th at o f

Jaggar and P a lach e (1905), who fir s t d escr ib ed th e Y avapai S c h is t and

m apped the r eg io n . Lindgren (1926) reco g n ized the v o lc a n ic and s e d i­

mentary nature o f th e rock s o f the Y avapai S c h is t . H e a ls o in v e s t ig a te d

many o f the su lfid e o ccu rren ces in th e s c h is t and co n c lu d ed th at the

copper m in era liza tio n w a s Precam brian in age and e p ig e n e t ic in o r ig in .

W ilso n (1939) corre la ted part o f the Y avapai S c h is t in the M ayer area

w ith the typ e s e c t io n o f th e Alder s e r ie s lo c a te d in the M a za tza l M oun­

ta in s 60 m ile s to the so u th e a s t . W ils o n 's Alder s e r ie s w a s m od ified to

the Alder Group by A nderson and C rea sey (1958), who su b d iv id ed the

Alder Group in to s ix form ation s, on e o f w hich i s th e T exas G ulch Forma­

t io n . Work by B la cet (1968) h a s s in c e show n th at the T exas G ulch

7

Form ation is much younger than the other rock s o f the Alder G roup. Be­

c a u s e the T exas G ulch Form ation w a s the k ey to corre la tin g the rock s o f

the M ayer area w ith the type Alder s e c t io n , W ilso n 's (1939) co rre la tio n

now appears in v a lid b e c a u se o f the s ig n if ic a n t age d if fe r e n c e . A nderson

e t a l . (1971) p rop osed renam ing the o th er fiv e form ation the Big Bug

G roup. G e o lo g ic quadrangle maps cover in g the w estern h a lf o f the M ayer

15-m inute quadrangle h ave b e e n recen tly p u b lish ed (Anderson and B la c e t ,

1972; A nderson , 1 9 7 2 ). E ven sen (1969) mapped th e cen tra l portion o f

the Agua Fria m ining d is tr ic t , w hich in c lu d e s th e C opper Q u een m in e,

and proposed the fo llo w in g c o n c lu s io n s , w hich are p ertin en t to th is

study;

1 . The rocks at the C opper Q ueen m ine w ere o r ig in a lly v o lc a n ic

rock s varying from rh yo lite to b a sa lt and g r a y w a ck es . T h ese

rock s w ere d e p o s ite d under su b aer ia l and subm arine c o n d it io n s .

2 . The rock s h ave b e e n stron g ly deform ed but w ere m etam orphosed

o n ly to lo w -g ra d e g r e e n s c h is t fa c ie s during th e M a za tza l R evo­

lu tio n 1 .3 7 to 1 .4 5 b .y . a g o .

3 . The ore body i s p o s t - fo l ia t io n and w a s formed in stru ctu ra lly

favorab le z o n e s by d e p o s it io n o f copper s u lf id e s that had b een

sc a v e n g e d from the country rock by hydrotherm al f lu id s .

GEOLOGIC SETTING

The C opper Q u een m ine o ccu rs on the e a ster n flank o f a s l ig h t ly

overturned sy n c lin e and b e tw een th e ea stern and w estern m argins o f the

S h ylock fau lt z o n e . The area i s co m p le te ly un derla in by Precam brian

rock s o f the Y avapai S e r ie s (F ig . 4 ) . The Y avapai S er ie s rock s w ere d e ­

p o s ite d during the in terv a l 1770 + 10 to 1820 m .y . ago (Anderson e t a l . ,

1971 , p . C - l ) . The rock s in the C opper Q ueen area are r es tr ic ted to the

Spud M ountains V o lc a n ic s . The Spud M ountains V o lc a n ic s , the younger

Iron King V o lc a n ic s , and the o ld er G reen G ulch V o lcan ics make up the

2 0 ,0 0 0 - fo o t - th ic k Big Bug Group (Anderson e t a l . , 1 9 7 1 ). The Iron King

and G reen G ulch V o lca n ics are predom inantly am ygd aloid and p illo w

b a s a lt s , w h ile th e Spud M ountain V o lca n ics are in term ixed rh y o lit ic and

a n d e s it ic p y r o c la st ic rock s w ith in terca la ted tu ffa ceo u s sed im entary

ro ck s . All rock s o f the Big Bug Group h ave undergone lo w -g ra d e reg io n a l

m etam orphism , but the p refix "m eta-" i s not u se d in d escr ib in g th e rock s

b e c a u se th eir o r ig in a l tex tu res are s t i l l v i s ib le .

Rock U n its

Spud M ountain V o lca n ics

The Spud M ountain V o lc a n ic s , w hich u n d erlies a lm o st th e e n ­

tire study area , i s here d iv id ed in to three m em bers, w hich h a v e lo c a l

mapping s ig n if ic a n c e . From o ld e s t to y o u n g e s t , th ey are th e r h y o lite -

d a c ite m em ber, the m arker-bed m em ber, and th e tu ff-b r e c c ia m em ber.

L ocal lith o lo g ic v a r ia tio n s are r ec o g n iz a b le in the r h y o lite -d a c ite and

8

EXPLANATION

BBG

IKV

iMS

SMS

3MV

GGV

BRADY BUTTE GRANODlORITE

TEXAS GULCH FORMATION

IRON KING VOLCANICS

SPUD MOUNTAIN SEDIMENTS

SPUD MOUNTAIN VOLCANICS

GREEN GULCH VOLCANfCS

S C A L EZ1 2 MILES

,SMV

' COPPER QUEEN MINE .

in

,

SMV

i- -rr,. * '* ■ .} & *

'GEOLOGY FROM ANDERSON and OREASEY(l958), ANDERSON et a l ( l97 l^

ANDERSON ond BLACET ( 1 9 7 4 ANDERSON (l972)

Figure 4 . Geology of the M ayer a rea , Yavapai County, Arizona

P R,E C AM

BR

I AN

tu ff-b r e c c ia mem ber, but the v a r ia tio n s are not o f su ff ic ie n t co n tin u ity

to be mapped s e p a r a te ly .

R h y o lite -D a c ite M em ber

The r h y o lite -d a c ite member i s ch a ra cter ized by an abundance o f

euhedral to round quartz p h e n o c r y s ts , ranging in s iz e from 3 to 10 mm,

in a l ig h t-c o lo r e d , f in e -g ra in ed m atrix (F ig . 5 ) . The un it crop s out in a

long ridge in the w estern part o f the stu d y area and forms part o f the

northern end o f the C opper Q u een ridge (F ig. 1 ). The rh y o lite s are lig h t

pink to b u ff, w h ile the d a c ite s are reddish v io le t to lig h t p u rp le . D a c ite

i s d is t in g u ish e d from rh y o lite by the p resen ce o f p la g io c la s e p h en o cry sts

and a d e c r e a se in quartz p h en o cry st c o n te n t . The un it i s probably 75 to

100 m eters th ic k .

In th in s e c t io n , the rh y o lite i s s e e n to c o n s is t o f 10 to 15 per­

c e n t euhedral to round quartz p h en o cry sts and 5 to 10 p ercen t o r th o c la se

fe ld sp a r p h en o cry sts in a groundm ass o f very fin e grained quartz and

s e r ic i t e . The quartz gra ins are com m only sh a ttered , w ith s e r ic ite f il lin g

the fr a c tu r es . C arlsb ad tw in n ing i s ev id en t in som e o f the larger fe ld sp a r

p h e n o c r y s ts , although s e r ic it iz a t io n h a s o b litera ted m ost fe ld s p a r s . The

f in e -g ra in ed s e r ic ite in the m atrix i s a lig n ed p a r a lle l to fo lia t io n p la n e s .

The d a c ite c o n s i s t s o f 10 to 15 p ercen t o l ig o c la s e p h en o cry sts

(M ichel-L dvy*s m eth od ), 5 p ercen t o r th o c la se p h e n o c r y s ts , and 5 per­

c e n t quartz p h en o cry sts in a very fin e grained groundm ass o f q u artz ,

s e r ic i t e , and probably o r th o c la s e . The p h en o cry sts are round to su b -

hedral and range in s i z e from 0 .2 5 to 3 mm. There h a s b een minor c h lo r -

it iz a t io n o f th e grou n d m ass, and the a lign m en t o f ch lo r ite and s e r ic ite

d efin e th e fo lia t io n w here th e rock i s s c h is t o s e .

10

Figure 5. Outcrop of rh y o lite -d ac ite member

Note the large quartz phenocrysts above p en c il.

Figure 6. Polished slab of specim en from m arker-bed member

Laminae are defined by varia tions in ch lorite co n ten t. Actual

12

M arker-bed M ember

The m arker-bed member i s a zon e o f th in ly la m in a ted , tu ffa -

c e o u s , sed im en tary rock s o v er ly in g the r h y o lite -d a c ite m em ber. T his

unit forms an e co n o m ic a lly s ig n if ic a n t and g e o lo g ic a lly im portant s tr a ti­

graphic h o r izo n . A ll ore at the C opper Q u een m ine o ccu rs in s u lf id e -

rich b a n d s, 2 to 5 cm th ick , w hich are restr ic ted to the rock s o f the

m arker-bed m em ber. The d is t in c t iv e lith o lo g y o f the member perm its i t s

u se as a marker bed in th e th ic k , fe a tu r e le s s v o lc a n ic s e c t io n .

The un it crop s out for more than 500 m eters on th e northern part

o f the C opper Q ueen ridge and a ls o on th e south ern part o f the B ingham p-

ton ridge (F ig . 1 ). The m arker-bed member i s seld om th ick er than 5 to 7

m e te r s . In o u tcro p , th e member i s co m p o sed o f very fin e g ra in ed , th in ly

b ed d ed , g reen ish to g reen ish -b ro w n , tu ffa ceo u s sed im en t bands (F ig . 6 ) .

In d iv id u al m ineral gra in s are seld om v is ib le to the unaided e y e , but a l ­

tern atin g , l ig h t - and d ark -green la m in a e , 0 .5 to 2 cm th ick , are e a s i ly

s e e n and , in fa c t , ch a ra cter ize the m em ber.

In th in s e c t io n , tw o m in era log ic a s se m b la g e s are r e c o g n iz a b le

in the m arker-bed m em ber. The first i s a lm o st en tire ly co m p osed o f very

fin e grained quartz and iro n -r ich c h lo r ite . The seco n d a sse m b la g e i s

com p osed o f a very fin e grained q u a r tzo -fe ld sp a th ic groundm ass c o n ­

ta in in g 25 p ercen t green ish -b ro w n se r ic ite or p o s s ib ly ferro stilp n o m el-

a n e . The c o lo r d ifferen ce th at d e fin e s the lam in ation s i s due to v a r ia ­

tio n s in ch lo r ite c o n te n t , darker bands havin g a greater co n cen tra tio n o f

ch lo r ite than lig h ter b a n d s . A lignm ent o f the p la ty m in erals forms the

fo lia t io n and is norm ally p a r a lle l to bedding e x c e p t in th e h in g e zo n e

o f the fo ld s w here fo lia t io n c u ts th e bedding at a n g le s up to 90 d e g r e e s .

13

S u lfid e -r ic h B a n d s. C opper su lfid e m in era liza tio n o f eco n o m ic

s ig n if ic a n c e i s r e s tr ic ted to th e m arker-bed m em ber. Figure 2 sh o w s the

sp a tia l re la tio n sh ip o f the ore w ith in the m arker-bed m em ber. It i s a ls o

apparent in Figure 2 that m in era liza tio n o ccu rs o n ly in s p e c if ic portion s

o f the m em ber. In th e ore z o n e , su lf id e m in era liza tio n i s con cen tra ted

in s i l ic e o u s b a n d s, 2 to 5 cm th ick , w hich are con tin u o u s a lon g strike

for up to 15 m eters (F ig . 7 a ) . T h ese su lf id e -r ic h bands co n ta in in g p y r ite ,

c h a lc o p y r ite , a r se n o p y r ite , s p h a le r ite , and ten n a n tite a ltern ate w ith

b ed s o f g reen tu ffa c eo u s se d im e n ts , 1 to 10 cm th ic k . The su lf id e c o n ­

ten t o f a band may be a s h igh a s 60 p ercen t by v o lu m e. In th e m in e, th e

su lf id e -r ic h bands are c o n s is t e n t ly p a r a lle l to the bedding in the e n c lo s ­

ing tu ffa c eo u s sed im en tary r o c k s , e v e n in a rea s w here in te n se fo ld in g

h a s b een im p osed on th e rock s (F ig . 7 b ) .

In p o lish e d s e c t io n , c h a lc o p y r ite , p y r ite , a r sen o p y r ite , sp h a l­

e r ite , a tan p h a se o f c h a lc o p y r ite , and ten n a n tite w ere id e n t if ie d . M in­

era l co n ten t i s v a r ia b le b e tw een b a n d s, but ch a lcp y r ite is g e n e ra lly th e

m ost abundant s u lf id e , forming about 50 p ercen t o f ea ch b an d 's su lfid e

c o n te n t . E stim ated r e la t iv e ab u n d an ces o f the other su lfid e m in era ls are

40 p ercen t p y r ite , 5 to 10 p ercen t a rsen o p y r ite , 1 p ercen t sp h a le r ite ,

l e s s than 1 p ercen t tan p h a se o f c h a lc o p y r ite , and l e s s than 0 .5 p ercen t

te n n a n tite . Figure 8 sh ow s a r ep resen ta tiv e a s se m b la g e o f the su lfid e

m in er a ls .

C h alcop yrite o ccu rs in te r s t it ia l to quartz gra in s a lon g th e e d g e s

o f the su lf id e -r ic h bands and form s a m atrix for the o th er su lfid e m iner­

a ls in the core o f the b a n d s . Anhedral b le b s range in s iz e from 0 .1 to 2

mm. S m all, 0 .1 to 0 .5 mm, anhedral b leb s o f sp h a ler ite and ten n a n tite

14

Figure 7. Sulfide-rich bands in the m arker-bed member

A. Sulfide-rich bands exposed in the 400 -leve l ore z o n e . B. Isoc lina l fold showing the c o n s is ten t para lle lism of su lfide-rich bands and sedim entary bedd ing .

15

Figure 8. Typical sulfide m ineral assem blage of ch a lco p y rite , p y rite , arsenopyrite , and sphalerite in su lfide-rich bands.

Reflected ligh t, SOX.

16

are in tim a te ly intergrow n w ith the ch a lco p y r ite and are a ssu m ed to be

e x so lu tio n fe a tu r e s . Twin la m e lla e w ere not s e e n in the ch a lco p y r ite

e v e n on e tch ed sp e c im e n s . Each grain appeared to be o p t ic a lly and

structura lly con tin u o u s and did not show any te x tu r e s , such a s p o ly g o ­

nal grain b o u n d a r ies, that are a s s o c ia te d with r e c r y s ta ll iz a t io n .

A tan p h a se o f ch a lco p y r ite occu rs a s d is t in c t , is o la te d gra in s

and in su b tle in tergrow ths w ith c h a lc o p y r ite . The co lo r o f the m ineral

i s a ssu m ed to r e f le c t an a b o v e -a v e r a g e selen iu m co n ten t in th e c h a lc o ­

pyrite (U ytenbogaardt and Burke, 1 9 7 1 ). There i s o n ly s lig h t v a r ia tio n

in the an iso trop ism o f th e tw o m in e r a ls , and d is t in c t io n b e tw een the

tw o i s o ften d if f ic u lt .

Pyrite and arsen op yrite occu r a s 0 .1 to 2 mm, euhedral c r y s ta ls

and anhedral fragm en ts, w hich are u su a lly e n c lo se d by a m atrix o f

quartz or c h a lc o p y r ite . C on cen tra tion s o f pyrite and arsen op yrite c a n

form d is t in c t la y ers w ith in a su lf id e -r ic h band, and both the band and

th e m ineral la y er are p a r a lle l to sed im entary bedding in th e e n c lo s in g

r o c k s . Pyrite w as a ls o o b serv ed as round gra ins up to 4 mm in d iam eter ,

w hich d isp la y growth z o n e s (F ig . 9 a ) . Each zon e i s marked by th e ter­

m ination o f p rism atic c r y s ta ls arranged ra d ia lly around the grain core

(F ig. 9 b ) .

Banded Iron F orm ation s. Prominent red ou tcrop s o f banded

iron form ations are strik ing fea tu res o f th e study area (F ig . 1 0 ). O ut­

crop s e x p o se d in th e w estern part o f the area occu r a s pod s a lon g the

c o n ta c t b e tw een the tu ff-b r e c c ia member and th e r h y o lite -d a c ite mem­

b er . Banded iron form ations a ls o crop ou t on th e m iddle and south ern

parts o f th e C opper Q u een r id g e , w here th ey rep resen t la tera l e x te n s io n s

17

Figure 9. Pyrite grains from su lfide-rich bands

A. U netched pyrite grain showing growth zones; reflec ted ligh t, 32X. B. Growth zones in unetched pyrite grain showing prism atic c ry s ta l term inations marking each zone; reflected ligh t, SOX.

18

Figure 10. Outcrop of banded iron formation

Outcrop shows strongly developed, southw est-p lunging lin e a - tion . Joints in outcrop are normal to fold axes in the banded iron for­m ation.

19

o f the m arker-bed m em ber. The red outcrops are co m p o sed o f sp e c u la r ite)

and qu artz.

In th in s e c t io n , th e banded iron form ations are co m p o sed o f

extrem ely fin e g ra in ed , 0 .0 1 mm or l e s s , quartz w ith f la k e s and sm all

b leb s o f sp e cu la r ite up to 0 .2 5 mm in s i z e . S p ecu la r ite -r ich bands are

dark gray and co n ta in about 40 p ercen t by volum e sp e c u la r ite .

T u ff-B reccia M em ber

The cen tra l and southern parts o f the stu d y area c o n ta in a s e ­

qu en ce o f in terbedd ed a n d e s it ic tu ffs and v o lc a n ic b r e c c ia s , here nam ed

th e tu ff-b r e c c ia m em ber, e stim a ted to be 110 m eters th ick . Angular frag­

m ents o f l ig h t-c o lo r e d a n d e s ite , 2 to 20 cm in d iam eter, in a d ark -green

a n d e s it ic m atrix ch a ra c ter ize th e v o lc a n ic b r e cc ia s (F ig . 1 1 a ) . The frag­

m ents are com m only e lo n g a te p a r a lle l to fo lia tio n and h ave b een nearly

ob litera ted in som e ou tcrop s by s lip a lon g c lo s e ly sp a c ed fo lia t io n

p la n e s . Along C opper Q u een r id g e , w here the rock s h av e b e e n s i l i c i f i e d ,

the b recc ia textu re i s not very e v id e n t . H ow ever , a p ercep tib le le n s o id -

a l pattern d e v e lo p s on w eath ered su r fa ces and r e f le c ts the fragm ental

nature o f the rock (F ig . l i b ) . Q uartz p h en o cry sts are v is ib le in o u tcro p ,

but th ey are much l e s s abundant and much sm a ller than the quartz p h en o­

c r y s ts in the r h y o lite -d a c ite m em ber. In the northern part o f the study

area , the b r e cc ia z o n e s show su b s ta n tia l d e c r e a s e s in fragm ent s i z e ,

th ic k n e s s , and r e la t iv e abundance w ith r e sp e c t to th e t u f f s . No b rec­

c ia s w ere found in the northern quarter o f the stud y a rea .

Interbedded w ith the b r e c c ia s are d ark -green a n d e s it ic tu f fs ,

w hich com m only c o n ta in c o n sp ic u o u s w hite o r th o c la se and p la g io c la s e

20

Figure 11. O utcrops of volcan ic b reccia of the tu ff-b recc iamember

A. U nsilic ified volcanic b reccia showing large angular frag­m ents. B. Fragment con ten t of s ilic if ie d volcanic b reccia reflected by the lenso ida l w eathering pa ttern developed on the outcrop su rfa c e .

21

p h en o cr y s ts . The tu ffs are m ost abundant in the northern part o f the area

and c o n s titu te about 60 to 70 p ercen t o f the rock in th e south ern area

w here th ey are in terbedd ed w ith the b r e c c ia s .

In th in s e c t io n , the tu ffs are s e e n to c o n s is t o f 60 p ercen t f in e ­

grained groundm ass co m p o sed o f 75 p ercen t s e r ic ite and 25 p ercen t

c h lo r ite . Anhedral quartz and o r th o c la se p h e n o c r y s ts , 0 .1 to 2 mm in

s i z e , co m p o se 5 p ercen t o f th e ro ck . The rem aining 25 p ercen t o f the

rock c o n s is t s o f o l ig o c la s e p h e n o c r y s ts , 1 to 2 mm in s i z e . Fragm ents

occurring in the b r e cc ia z o n e s h a v e co m p o sitio n s s im ilar to th at o f the

t u f f s . W here fo lia t io n i s w e ll d e v e lo p e d , it i s d efin ed by th e a lign m en t

o f p la ty m in era ls and e lo n g a te fra g m en ts .

Quartz V eins

L arge, m a s s iv e ou tcrop s o f barren w h ite quartz are w e ll e x ­

p o se d in the stu d y area (F ig. 1 ) . Sm aller v e in s o f q u artz, w hich c r o s s

a ll u n its , w ith the p o s s ib le e x c e p t io n o f the d ia b a se , w ere o b serv ed in

th e mine w o rk in g s . Shear z o n e s and som e sm a ll fa u lts in th e mine w ork­

in g s are ch a ra cter ized by q u a r tz - f ille d fra c tu res . Some v e in s c o n ta in

rare b le b s o f pyrite and c h a lc o p y r ite , but m ost are barren.

D ia b a se D ik e s

D ia b a se d ik e s , ranging in w idth from 0 .3 to 1 m eter, crop ou t

in the stud y area (F ig s . 1 and 2 ) . The d ik es w eath er e a s i ly and are com ­

m only d if f ic u lt to s e e , a s th ey are ty p ic a lly co v ered by ru b b le. Under­

ground ex p o su res are e x c e l le n t , and the rock i s s e e n to c o n s i s t o f 2 -

mm a u g ite and p la g io c la s e gra in s intergrow n in a ty p ic a l d ia b a s ic t e x ­

tu re . There are o c c a s io n a l , 5 - to 15-mm eu h ed ral a u g ite and b io t ite

22

c r y s ta ls in the d ik e s . The d ik e s are not fo lia te d , and th ey do not prefer­

e n tia lly intrude a long fo lia t io n p la n e s . The d ia b a se d ik es apparently

cu t a ll other rock u n its in th e a r ea . E ven sen (1969) co n c lu d ed th at the

d ik es are Tertiary in a g e and are re la ted to the nearby H ick ey b a s a lt

f lo w . The d ik es h a v e not b een rad iom etr ica lly d a te d .

Structural F eatu res

Shy lo ck F au lt Zone

The Sh ylock fau lt i s a m ajor structure o f Precam brian a g e .

A nderson and C rea sey (1958) note that th e fa u lt i s co v ered by u n d is­

turbed T apeats S an d ston e o f Cam brian a g e a t M ingus M ountain , 18 m ile s

north o f th e stud y a rea . Anderson (1972) d e sc r ib e s the S h y lock fa u lt a s

a major structural fea tu re , 45 m ile s lo n g , w ith a s much a s 5 m ile s o f "

r ig h t- la te r a l s l i p . E vid en ce for th is d isp la cem en t c o n s is t s o f o f f s e t

s l i c e s o f quartz d iorite in th e M ingus M ountain a r ea . In the C opper

Q ueen mine a rea , th e fa u lt w id en s in to a zon e a m ile w id e , w ith the

C opper Q ueen m ine ly in g b e tw e en the e a ste r n and w e stern m argins o f

the fau lt z o n e . The e a ster n m argin o f the zon e l i e s in Bear Track C an­

y o n , a w e ll-d e v e lo p e d , so u th ea st-tren d in g lin ea r drainage near the

ea stern ed ge o f the stu d y area (F ig. 1 ). The w e ste r n m argin i s ju s t w e s t

o f the m apped a r ea . Rocks e a s t and w e s t o f th e fau lt zo n e are much l e s s

fo lia ted and sh eared than rock s ly in g w ith in the z o n e . O utcrops o f th in ,

w e ll-d e f in e d , graded b ed s are com m on o u ts id e the fa u lt z o n e , w h erea s

such primary d e p o s it io n a l fea tu res are rare w ith in the fa u lt z o n e . D is ­

p la cem en t a lon g th e e a s te r n m argin o f th e fa u lt zo n e c o n s is t s o f

le ft-h a n d ed sep a ra tio n o f sed im en tary b ed s along N . 15o - 2 0 ° W .

str ik in g , v e r t ic a lly dipping p la n e s .

Hum boldt S y n clin e

A major so u th -p lu n g in g sy n c lin e is d efin ed by the northward

co n v erg en ce o f the Spud M ountain and Iron King V o lca n ics (F ig . 2 ) .

T his fo ld i s here nam ed th e Hum boldt sy n c lin e a fter the sm a ll tow n o f

H um boldt, w hich l i e s c lo s e to th e a x ia l trace o f the fo ld . To determ ine

the geom etry o f the s y n c lin e , bedd ing a ttitu d es (F ig . 12) and a x e s o f

minor fo ld s (F ig . 13) w ere co m p iled for the area o f Figure 4 . F o ld s w ere

exam ined in the Power Line G ulch and Blue B ell l o c a l i t i e s , and the fo ld s

ca n be d e sc r ib e d , u s in g F leu ty 's (1964) c la s s i f i c a t io n , a s s l ig h t ly o v er­

turned, tig h t to is o c l in a l w ith m oderate to s te e p ly p lunging a x e s . A s­

sum ing that p a r a s it ic fo ld s r e f le c t the geom etry o f a larger s c a le fo ld ,

th e Hum boldt sy n c lin e i s an is o c l in a l fo ld w ith a s l ig h t ly overturned

w estern lim b and a m od erately p lunging a x is .

F o lia tio n

F o lia tio n i s th e m ost p en etra tiv e and p e r v a s iv e e lem en t o f th e

lo c a l structural fabric and i s strongly d ev e lo p ed in a lm o st ev ery ou t­

crop . F o lia tio n i s d efin ed by th e p a r a lle l a lign m en t o f s e r ic ite and

ch lo r ite in a l l rock s o f th e stu d y a rea . The v o lc a n ic b r e c c ia s d isp la y

fla tten in g and e lo n g a tio n o f rock fragm ents p a r a lle l to fo lia t io n . Al­

though n orth east and north w est a ttitu d es are com m on, fo lia t io n i s ch ar­

a c ter ized by n o r th -str ik in g , 8 0 ° W . -d ip p in g p la n e s (F ig . 1 4 ). A n a ly s is

o f m e so sc o p ic fo ld s in th e stu d y area in d ic a te s th at the fo lia t io n i s c o ­

in c id en t w ith th e a x ia l su r fa c es o f the fo ld s (t"ig. 1 5 ).

23

24

N

Figure 12 . Lower hem isph ere p o le -d e n s ity diagram o f p o le s to bedding for the M ayer area

Contour v a lu e s eq u al 0%, 5%, 10%, and 20%; 103 r e a d in g s .

Figure 1 3 . Lower h em isp h ere p o le -d e n s ity diagram o f a x e s o f minor fo ld s for the M ayer area

Contour v a lu e s eq u a l 0%, 5%, 10%, and 20%; 43 r ea d in g s .

25

Figure 14 . Lower h em isp h ere p o le -d e n s ity diagram o f p o le s to fo lia t io n at the C opper Q u een m ine area

C ontour v a lu e s eq u a l 0%, 5%, 15%, and 25%; 78 r e a d in g s .

Figure 15 . Lower h em isp h ere p o le -d e n s ity diagram o f p o le s to a x ia l su r fa c es for a l l fo ld s m easured in the M ayer area

C ontour v a lu e s eq u a l 0%, 5%, 10%, and 25%; 104 r e a d in g s .

26

F o lia tio n a ls o d e fin e s a su rface a lon g w hich m ovem ent h a s

tak en p la c e . Fold lim bs are com m only cu t by s lip su r fa ces a long w hich

tra n sp o s itio n o f bedd ing h a s occu rred (F ig , 1 6 ). E vid en ce for tr a n sp o s i­

tio n can be s e e n in th e sm a ll, t ig h tly c o m p r e ssed , r o o t le s s fo ld s show n

in Figure 17 and in the outcrop pattern on Figure 1 . South o f the B in g-

ham pton m ine near the o ld m ill s it e i s a sou th -p lu n g in g a n t ic lin e w ith

an apparently w a v e len g th o f about 30 m e te r s . The a x ia l trace o f th is

fo ld h a s b een c o n s is t e n t ly o f f s e t a lon g fo lia t io n p la n es in a le ft-h a n d e d

s e n s e . The resu ltin g tra n sp o s itio n o f bedding c r e a te s th e ap p earan ce o f

a refo ld ed fo ld .

F o lia tio n o f Su lfid e M inera ls

F o lia tio n o f su lfid e m in era ls i s p reva len t in som e sp e c im en s

from the ore body and o n ly poorly d ev e lo p ed or a b sen t in o th e r s . The

fo lia tio n i s d efin ed by (1) a lig n ed pyrite fragm en ts, (2) ch a lc o p y r ite

la m in a e , and (3) c h a lco p y r ite p ressu re sh a d o w s .

Pyrite gra in s th a t h a v e b een broken and ex ten d ed a lon g fo l ia ­

tio n p la n es are com m on in th o se sp ec im en s co n ta in in g fo ld h in ge z o n e s .

T h ese large gra ins are broken in to a m osa ic o f angular fragm ents com ­

m only sep arated by c h a lc o p y r ite . Figure 18 sh ow s a zo n ed p yrite gra in

that h as b een broken and ex ten d ed along fo lia t io n p la n e s . O ther large

grains o f pyrite show str in gers o f a lig n ed pyrite fragm ents " tra ilin g

away" from the parent gra in .

C h a lcop yrite o ccu rs a s s m a ll, th in , le n s -s h a p e d la m in a e ,

w hich are conform able w ith the fo lia t io n (F ig. 1 9 ). The ch a lco p y r ite

lam inae and the fo lia t io n in the w a ll rock are p a r a lle l both to bedding

and su lf id e -r ic h b a n d s , e x c e p t w here fo ld in g h a s b e e n im p osed on the

27

Figure 16. Fold limbs in sedim entary rocks cut by tra n sp o s i­tion along ax ia l-p lan e fo lia tion

Figure 17. C losely spaced slip surfaces which have alm ost- formed ro o tle ss folds in thinly bedded sedim entary rock

28

Figure 18. Fragmented zoned pyrite grain with fragm ents extended p a ra lle l to fo lia tion

Figure 19. C halcopyrite lam inae concordant with fo liation .

Note p ressu re shadows of chalcopyrite around pyrite g ra in s . Reflected ligh t, 32X.

29

r o c k s . In th e f o ld s , th e fo lia t io n and lam inae a ssu m e an a x ia l planar re ­

la tio n sh ip to the fo ld ed b e d s . Pyrite grains w ith in th e ch a lco p y r ite lam ­

in ae form the core o f th e su lfid e le n s . C h alcop yrite p ressu re sh ad ow s

com m only occu r on e ith er s id e o f th e pyrite grain (F ig. 2 0 ) . T h ese p r e s­

sure sh ad ow s are a ls o p a r a lle l to the fo lia t io n .

Bedding

Sedim entary rock s th at d isp la y w e ll-d e v e lo p e d bedding are not

abundant in the stu d y a r ea . Bedding i s reco g n iza b le in th e m arker-bed

member and in the banded iron form ations and forms su r fa ces that h a v e

recorded the deform ational h is to ry o f the r o c k s . Bedding a ttitu d es for

the study area are d isp la y e d a s a p o le -d e n s ity diagram (F ig. 2 1 ) . This

diagram r e v e a ls a s ta t is t ic a l ly preferred bedding or ien ta tio n o f N . 1 0 ° E . ,

8 0 ° W .

Graded bedding perm its determ ination o f stra tigrap h ic top w ith ­

in som e portion s o f the sed im entary rock s o f th e C opper Q u een a r ea .

M ost o f the bedding o b serv ed in th e stud y area d ip s w e s t and is right

s id e u p . Graded bedding i s d efin ed in th e m arker-bed member by v a r ia ­

tio n s in ch lo r ite c o n te n t . The b a se o f m ost lam inae ca n be reco g n ized

in th in s e c t io n by the co n cen tra tio n o f c h lo r ite , w hich d e c r e a s e s tow ard

the to p . The upper parts o f the lam in ae are com p osed predom inantly o f

f in e -g ra in ed quartz w ith very l i t t le c h lo r ite . Lavery (1972) h a s u se d the

ch lo r ite co n ten t o f lam inae a s graded bedding in d ica to rs in Arche an v o l­

c a n ic r o c k s .

O verturned bedding w a s a ls o o b serv ed in the stu d y a r ea . T h ese

b ed s dip s te e p ly w e s t and g e n e ra lly o ccu r on the e a ste r n lim b o f s lig h t ly

30

Figure 20. P ressure shadow of chalcopyrite around zoned pyrite grain

SOX.C halcopyrite len ses are p a ra lle l to fo lia tion . Reflected ligh t,

31

N

Figure 2 1 . Lower h em isp h ere p o le -d e n s ity diagram o f p o le s to bedding for the C opper Q ueen mine area

C ontour v a lu e s eq u a l 0%, 5%, 10%, and 25%; 43 r e a d in g s .

32

overturned f o ld s . Bedding and fo lia t io n a ttitu d es are nearly id e n t ic a l

throughout the stud y a r ea . H ow ever , fo lia t io n tr a n se c ts bedding in the

h in ge zon e o f f o ld s . W here bedding and fo lia t io n in te r s e c t , a lin e a t io n

i s produced th at co rresp on d s in a ttitud e to the trend and p lu nge o f the

fold a x e s .

F olds

R ocks o f the C opper Q u een area h av e b een deform ed in to m ega­

s c o p ic , m e s o s c o p ic , and m icro sco p ic f o ld s . M eg a sc o p ic fo ld s h a v e a

w a velen gth o f app roxim ately 300 m eters and stron g ly in flu en ce th e ou t­

crop p attern , as show n in Figure 1 . M eg a sc o p ic s y n c lin e s and a n ti­

c l in e s are d efin ed by th e co n v erg en ce and c lo su r e o f th e rock u n i t s .

W e ll-d e v e lo p e d m e so sc o p ic fo ld s occu r throughout the stu d y area on

th e flan k s o f the m e g a sc o p ic fo ld s but are m ost abundant in th e h in g e

z o n e s o f the larger f o ld s . M e s o s c o p ic fo ld s are b e s t d ev e lo p ed in the

bedded rock s o f th e m arker-bed member and the banded iron fo rm a tio n s .

Folds w ere not o b serv ed in the th ick v o lc a n ic u n it s . Kink fo ld s h avin g

am plitudes o f about 1 mm w ere o b serv ed in th in s e c t io n . Three d is t in c t

ty p es o f fo ld s are o b serv ed in the stu d y area: (1) i s o c l in a l fo ld s , (2)

tig h t asym m etric f o ld s , and (3) kink fo ld s .

1 . I s o c lin a l fo ld s are w e ll d ev e lo p ed in the m arker-bed member

(F ig . 2 2 ) . The am plitude o f m e so sc o p ic fo ld s seld om e x c e e d s

3 m e te rs , and w a v e len g th s are l e s s than 1 m eter . If a s im ila r

ratio b e tw e en am plitude and w a v e len g th e x is t s for th e m ega­

sc o p ic f o ld s , fo ld s h av in g a w a v e len g th o f 300 m eters w ould

h a v e an e x p e c te d am plitude o f 900 m e te rs .

33

Figure 22. M esoscopic iso c lin a l fold with tigh t asym m etric p a ra s itic folds in the m arker-bed member

Axial surface of folds dips w e st.

34

2 . Tight asym m etric fo ld s com m only occu r in the lim bs o f i s o c l in a l

fo ld s (F ig . 2 2 ) . A n tic lin es ty p ic a lly h a v e a s te e p ly d ip p in g ,

s lig h t ly overtu rn ed , e a ster n lim b and a sh a llo w er dipping w e s t ­

ern lim b . Fold am p litu d es are g en era lly l e s s than 50 cm , and

w a v e len g th s are l e s s than 25 cm .

3 . Kink fo ld s are d efin ed in the study area by fo ld ed fo lia t io n sur­

f a c e s . They are ty p ic a lly sm a ll, w ith am p litu d es l e s s than 10

cm , and h a v e sh arp , angular h in ge z o n e s (F ig . 2 3 ) .

Folds in S u lfid e -r ich Bands

O f particu lar im portance to th is study are th e s t y le and o r ien ta ­

tio n s o f fo ld s in the su lf id e -r ic h b a n d s. Various lo c a l i t ie s in the mine

w orkings provide e x c e l le n t ex p o su res o f fo ld ed su lf id e -r ic h bands in

w hich the a ttitu d es o f 41 fo ld a x e s and a x ia l su r fa c es w ere m easu red .

Figure 24 sh ow s w e ll-d e v e lo p e d is o c l in a l fo ld s in su lf id e -r ic h bands

e x p o sed in th e north fa ce o f the r a ise co n n ec tin g the s to p e s from the

400 le v e l w ith the 300 le v e l (F ig. 2 ) . T ight asym m etric fo ld s in the

su lf id e -r ic h bands w ere found to d isp la y a c o n s is t e n t Z sh ap e w hen

v iew ed down the fo ld a x is . Both lim bs o f su ch fo ld s dip w e s t , w ith

the e a s t lim bs o f the a n tic lin e ty p ic a lly overtu rn ed .

Fold M orphology

The m orphology o f the fo ld s in the stud y area i s d e scr ib ed

u sin g th e c la s s i f i c a t io n s o f Ram say (1967) and H u d le sto n (1 9 7 3 ).

H u d lesto n h a s co n stru c ted 30 id e a liz e d fo ld h in g e z o n e s b a se d on var­

ia t io n s in fo ld "shape" and "am plitude (F ig . 2 5 ) . By com p arison o f

p ro file s o f in d iv id u a l fo ld su r fa c es w ith H u d le sto n 's m od el, a

35

Figure 24. Iso c lin a l folds in su lfid e-rich bands exposed in ra ise betw een 400 and 300 le v e ls , Copper Q ueen mine

36

Figure 2 5 . H u d le sto n 's c la s s i f ic a t io n o f fo ld forms

C la s s if ic a t io n sh o w s 30 id e a l fo ld form s, d efin ed b e tw een in ­f le x io n and h in g e p o in ts: 6 c a te g o r ie s o f " sh a p e ," A-F; 5 c a te g o r ie s o f "a m p litu d e ," 1 - 5 . From .H u d lesto n (1973 , p . 1 3 ).

o

o o

ooo ooooo oo ooooooo ooooqooo0

oo ooo ooooooooo ooooooooooooooooo

Figure 2 6 . C om p ila tion o f fo ld forms for C opper Q u een m ine area , b a sed on H u d le sto n 's c la s s i f i c a t io n

37

s ta t is t ic a l ly preferred fo ld m orphology w as determ ined for the study a rea .

C om parison o f 63 h in ge z o n e s w ith th e m odel (F ig. 26) in d ica ted th at

shape 5E i s the m ost com m on in the stud y a rea .

R am say's (1967) a n a ly s is o f th e re la tio n sh ip b e tw een th e upper

and low er su r fa ces o f a fo ld ed la y er im p o ses m athem atica l param eters on

the c la s s i f i c a t io n o f fo ld m orph ology . The is o c l in a l and tig h t asym m etric

fo ld s o f the stu d y area approxim ate R am say's s u b c la s s 1C , w hich is

ch a ra cter ized by the orthogon al th ic k n e ss o f th e fo ld ed la y er b ein g

greater in the h in g e zon e than on the flan k s o f the fo ld . The kink fo ld s

approxim ate c la s s 2 f o ld s , w h ich h ave a co n sta n t orthogonal th ic k n e ss

o f the fo ld ed layer throughout the fo ld .

F o ld -a x is O rien tation

Lower h em isp h ere , eq u a l-a re a p ro jectio n s o f m e so sc o p ic fo ld

a x e s in the stud y area (F ig. 27a) show a strong unim odal d istr ib u tio n

o f p o in ts . The s te e p so u th w est p lu n ge o f the fo ld a x e s i s a lm ost id en ­

t ic a l to th e p lu n ge o f the H um boldt sy n c lin e and it s a s s o c ia te d minor

fo ld s (F ig. 1 3 ). The d istr ib u tion o f fo ld a x is o r ien ta tio n s for the fo ld ed

su lf id e -r ic h bands (F ig . 27b) a ls o sh o w s a trend and p lu nge s im ilar to

th at o f the reg io n a l s tru c tu re . Figure 27c i s a p o le -d e n s ity diagram for

a ll fo ld a x e s m easured in th is stu d y . The a x e s show a str ik in g unim odal

o r ien ta tio n o f S . 1 0 ° W . at 6 0 ° .

F au lts

F au lts are an in teg ra l and p e r v a s iv e e lem en t in the structural

fabric o f the stud y a rea , but th eir a lign m en t p a r a lle l to bedding and

fo lia t io n m akes d isp la ce m e n t d if f ic u lt to d e te c t and m ea su re . F au lts

38

N

Figure 2 7 . Lower h em isp h ere p ro jec tio n s o f fo ld a x e s

a . Fold a x e s m easured in the C opper Q u een m ine a r ea . C on ­tour v a lu e s eq u a l 0%, 5%, 15%, and 30%; 48 rea d in g s .

b . Fold a x e s o f s u lf id e -r ic h b a n d s . Contour v a lu e s eq u a l 0%, 5%, 15%, and 30%; 41 r e a d in g s .

c . A ll fo ld a x e s m easured in the M ayer a r ea . Contour v a lu e s are 0%, 5%, 15%, and 20%; 129 r e a d in g s .

39

cu t a c r o ss fo ld s , fo lia t io n , and a ll rock u n its e x c e p t the d ia b a se d ik e s ,

w hich com m only occu r in inferred fa u lt z o n e s . D isp la c em en t a lon g

fa u lts i s b e s t o b serv ed in th e underground w orkings o f the C opper Q ueen

m in e, w here fau lt p la n es and sep a ra tio n fea tu res h ave not b een o b liter ­

ated by w ea th er in g .

A ll fa u lts exam ined w ere found to ex h ib it r ev erse sep a ra tio n .

R everse fa u lts th at d isp la y major sep a ra tio n str ik e north to N . IQO E.

and dip s te e p ly w e s t or, l e s s com m only, e a s t . R everse fa u lts that d i s ­

p la y on ly minor sep a ra tio n o f l e s s than 1 m eter str ik e N . 10o - 2 0 ° W .

and dip 4 0 ° - 5 5 ° W . The e a s t , or fo o tw a ll, c o n ta c t o f the ore zon e i s

c o n s is t e n t ly marked by a w e s t-d ip p in g rev erse fa u lt , w h ich i s g e n e ra lly

p a r a lle l to fo lia t io n (F ig . 2 ) . F a u lts tra n sv erse to fo lia t io n do occu r in

the study area and d is p la c e l ith o lo g ic c o n ta c ts (F ig . 1 ) . T ran sverse •

fa u lts in the m ine do not d is p la c e the m arker-bed member and are a s ­

sum ed to m erge w ith the rev erse fa u lts that com m only bound the m arker-

bed m em ber.

Joints

D isco n tin u o u s curvip lan ar jo in ts are com m on in the rock s o f

the study area but do not show a reg io n a l pattern (E ven sen , 1 9 6 9 ). H ow ­

e v e r , in areas o f in te n se fo ld in g , su ch a s C opper Q u een r id g e , co n tin u ­

o u s planar jo in ts h a v e d e v e lo p e d . T h ese jo in ts str ik e N . 60o - 8 0 ° W .

and dip 20o - 4 0 ° NE. This a ttitu d e is approxim ately normal to the fo ld

a x e s th at are e x p o sed in the sam e outcrops (F ig. 11) and in d ic a te th at

th e jo in ts are c r o s s or e x te n s io n jo in t s .

40

L ineation

The predom inant lin e a t io n o b serv ed and m easured in th e study

area i s d efin ed by e lo n g a te m ineral g r a in s . F eld sp ar p h en o cry sts are

com m only e lo n g a te a long fo lia tio n p la n es and h av e an average trend

and plunge o f 6 0 ° S . 2 0 ° W . M in era ls , su ch a s c h lo r ite , th at h ave re­

c r y s ta ll iz e d in a preferred or ien ta tio n on the fo lia t io n p lan e h av e a s im i­

lar trend and p lu n g e . In g e n e ra l, the or ien ta tio n o f m ineral lin e a t io n s is

nearly id e n t ic a l w ith the or ien ta tio n o f fold a x e s in th e stud y a rea .

PRECAMBRIAN HISTORY OF THE REGION

The g e o lo g ic h is to ry o f Precam brian rock s in Arizona i s not com

p le te ly u n d erstood , but su ff ic ie n t work h as b een done to perm it the d e ­

velop m en t o f a p la u s ib le m odel for the d e p o s it io n and su b seq u en t

deform ation o f rock s o f th e Y avapai S e r ie s .

D e p o s it io n o f the Y avapai S er ies

During Y avapai S e r ie s tim e , 1820 to 1770 m .y . a g o , A rizona

w a s the s i t e o f a major g e o sy n c lin e (S chuchert, 1 9 2 3 ). The sed im en ts

in the M a za tza l M ountains rep resen t a d e lta d e p o s it accu m u lated on the

m argins o f the g e o s y n c lin e (W ilson , 1 9 6 2 ). N orth w est o f the sh o re lin e

som e 70 to 90 m ile s w a s a n orth east-tren d in g c h a in o f v o lc a n o e s . The

rock s o f the C opper Q u een m ine area w ere d e p o s ite d presum ably by th is

v o lc a n ic s y s te m . P illow b a s a lts w ere d e p o s ite d in th e m arine b a s in s

ad ja cen t to the v o lc a n o e s . The graded sed im entary bedd ing a ls o in d i­

c a te s a su b aq u eou s d e p o s it io n a l environm ent (Anderson and C r e a s e y ,

1 9 5 8 ). P o s s ib ly s im u lta n eo u s w ith th e d e p o s it io n o f in terca la ted v o l­

c a n ic flo w s and tu ffa c eo u s sed im en ts o f the Spud M ountain V o lca n ics

w a s the in tru sion o f th e Brady Butte G ran od iorite . M inor u p lift and

ero s io n e x p o se d th is p lu to n , w hich w a s th en co v ered by the sed im en ­

tary and v o lc a n ic rock s o f the T exas G ulch Form ation (Anderson and

B la c e t , 1 9 7 2 ). The T exas G ulch Form ation i s the y o u n g es t Precam brian

form ation in the M ayer area th at w a s a ffec te d by fo ld in g .

41

42

The M a za tza l R evolution

The M a za tza l R evolution (W ilson , 1 9 3 9 , 1962) h a s b een a s ­

s ig n ed to the tim e in terv a l o f 1 .2 to 1 .5 b . y . a g o . The rev o lu tio n w as

co n sid ered to be a reg io n a l te c to n ic ev en t and is d e scr ib ed by W ilso n

(1962, p . 12 -13) a s fo llo w s:

R eg io n a lly , the M a za tza l R evolu tion produced major fo ld in g and fo lia t io n or s c h is t o s i t y w h ich trend p rev a ilin g ly north­e a s t and lo c a lly north or northw estw ard; minor fo ld in g . . . o f w e s t and northw estw ard trends; thrust fa u lts and s te e p rev erse fa u lts w hich strik e approxim ately p a r a lle l to th e fo ld s; sh ea r fa u lts o f g en era l north -sou th and e a s t - w e s t trends; and s te e p n orth w esterly fa u lt s .

W ilso n further s ta te d th at after the M a za tza l R evo lu tion , th e Jerom e-

M ayer area w as su b jec ted to a prolonged period o f e ro s io n after w hich

the younger Precam brian A pache Group w as d e p o s ite d . H o w ever , A p ach e-

age rock s are a b sen t in the Jerom e-M ayer area and the T apeats S an d ston e

o f Cam brian age r e s ts on the fo ld ed o lder Precam brian r o c k s .

The Grand C anyon D istu rb an ce

N ear the end o f younger Precam brian tim e , another te c to n ic

ev en t w a s im p osed on the rock s (W ilson , 1 9 6 2 , p . 17):

Younger Precam brian tim e in Arizona approached an end w ith a period o f structural deform ation , g e n e ra lly know n a s the Grand C anyon D is tu rb a n ce , w hich cu lm in ated w ith e x te n s iv e in tru sion by d ia b a s ic s i l l s and d ik e s . T his deform ation i s e x p r e s se d in structural fea tu res o f ty p e s and trends s im ila r to th o se o f the M a za tza l R evolu tion , a lthough o f much w ea k ­er d ev e lo p m en t.

T his w a s the la s t s ig n if ic a n t te c to n ic ev en t to a ffe c t the rock s o f the

Jerom e-M ayer a rea , a s the P a le o z o ic s e c t io n at Jerome is s e e n to r e s t

undisturbed on stron g ly deform ed, o ld er Precam brian r o c k s .

GEOLOGIC HISTORY OF THE COPPER QUEEN MINE AREA

The rock s in the C opper Q ueen mine area rep resen t o n ly a sm all

fraction o f th e to ta l th ic k n e ss o f th e rock s d e p o s ite d as a r esu lt o f P re-

cam brian v o lc a n ic a c t iv ity in the M ayer a rea . H o w ever , th ey are s ig ­

n ifica n t in th at m a ss iv e su lfid e ore b o d ie s occu r w ith in a lim ited

stratigraphic h o r izon w ith in th e s e ro ck s . S p e c if ic a lly , a l l econ om ic

m in era liza tio n in the stud y area d irectly o v e r lie s the r h y o lite -d a c ite

member o f the Spud M ountain V o lcan ics and is co n ta in ed w ith in the

m arker-bed m em ber.

D e p o s it io n o f the R h y o lite -D a c ite M ember

The r h y o lite -d a c ite member i s an accu m u lation o f f lo w s and

p y r o c la st ic d e b r is , w hich formed a la te r a lly con tin u o u s un it and lo c a l

d o m es. Z ones o f in c r e a se d p y r o c la s t ic c o n ten t, su ch a s th e northern

end o f C opper Q u een r id g e , are in terp reted to be a part o f such d o m es.

Other rh y o lit ic m a s s e s crop out in the reg ion and h a v e a geom etry and

stratigraphy w hich are c o n s is t e n t w ith th e dome in terp reta tio n . The

v e n ts that formed th e dom es are interpreted to be part o f an a c t iv e , su b ­

marine v o lc a n ic fum arolic co m p lex .

D e p o s it io n o f the M arker-bed M em ber

After d e p o s it io n o f the r h y o lite -d a c ite m em ber, v o lc a n ic a c ­

t iv ity su b sid ed and a period o f r e la t iv e q u ie s c e n c e e n su e d , w hich

w a s marked by the d e p o s it io n o f th e very fin e g ra in ed , tu ffa c eo u s

43

44

sed im en ts o f the m arker-bed m em ber. The rock s o f th is un it h ave an ap­

pearance and co m p o sitio n th at may be ex p la in ed by the c h em ica l p rec ip ­

ita tio n o f a s i l ic e o u s rock from s e a w ater .

The la tera l gradation o f the m arker-bed member in to a banded

iron form ation in d ic a te s that both rock ty p es w ere accu m ulating s im u l­

ta n e o u s ly . The m arker-bed member and the banded iron form ation c o n ­

stitu te and lith o lo g ic and tem poral un it d isp la y in g a zon in g o f iron

m ineralogy id e n t ic a l to th e zon in g proposed for banded iron form ations by

James (1954). Jam es h a s d is c u s s e d in d e ta il the c o n c ep ts d ea lin g w ith

th e g e n e s is o f banded iron form ations in w hich h e a sc r ib e s th eir orig in

to ch em ica l p rec ip ita tio n o f iron and s i l i c a from s e a w a ter . H o w ev er ,

th e minimum iron co n ten t o f 15 p ercen t for banded iron form ations (G ross,

1965) e lim in a te s cer ta in portion s o f the m arker-bed member from the

banded iron form ation c la s s i f i c a t io n . To avoid the e x c lu s io n o f rock s

that are o b v io u s ly g e n e t ic a lly re la ted from an arbitrarily d efin ed c l a s ­

s if ic a t io n , Ridler (1973 , p . 59) h a s proposed th e term " e x h a lite s ,"

w hich "are the c la s s o f ch em ica l sed im en ts o f predom inantly v o lc a n ic

o r ig in ." The rocks o f the m arker-bed member and the banded iron for­

m ations are p la ced under the more gen era l term " exh alite" in th is

s tu d y .

E x h a lites c a n h av e up to four r ec o g n iz a b le c h em ica l fa c ie s in

w hich the iron occu rs e ith er as an o x id e , s u lf id e , s i l i c a t e , or carb onate

m in era l. M in era log ic zon in g is u su a lly d ev e lo p ed around an area h avin g

a red ucing environm ent, w hich c a u s e s th e p rec ip ita tio n o f th e su lfid e

f a c ie s , u su a lly p y r ite . The su lfid e fa c ie s ca n grade la te r a lly in to the

s i l ic a t e or carb onate f a c ie s , w hich are ch a ra cter ized by ch lo r ite and

45

s id e r ite , r e s p e c t iv e ly . The o x id e fa c ie s co m p r ises the outerm ost zo n e

o f the seq u en ce and i s co m p osed o f ch ert, ja sp e r , h em a tite , and m ag­

n etite . The co m p o sitio n o f the iron m ineral p rec ip ita ted in ea ch zo n e

r e f le c ts the Eh-pH co n d it io n s at th e tim e o f d e p o s it io n . The e x h a lit e s

o f the M ayer area h av e b een stu d ied in som e d e ta il (Brook, 1973), and

c h a n g e s in th e norm ally o x id iz in g d e p o s it io n a l environm ent are attributed

to lo c a l fum arolic v e n ts that in trod uced sulfur in to the s y s te m . At the

C opper Q ueen m in e, the ore zo n e co m p r ises th e su lfid e f a c i e s . The

ore zo n e grad es la te r a lly in to the s i l ic a te fa c ie s com p osed o f s i l ic e o u s

c h lo r it ic r o c k s . The carb onate fa c ie s i s not a lw a y s p resen t a s a w e l l -

d efin ed z o n e . M ixtures o f carb onate and su lfid e fa c ie s m in erals w ere

ob serv ed in th e underground w o rk in g s. M a ss iv e carb onate fa c ie s rock s

are show n o n Figure 1 , but th eir sp a t ia l re la tio n sh ip w ith the o th er fa c ie s

o f the e x h a lite i s o ften d if f ic u lt to d eterm in e . The o x id e fa c ie s i s ch ar­

a c ter ized by the large prom inent ou tcrop s o f ch er t, ja sp e r , and sp ecu la r

h e m a tite .

The v a rv e lik e appearance o f bedding in th e m arker-bed member

i s c a u sed by va r ia tio n in ch lo r ite c o n te n t . Lavery (1972) h as exam ined

other Precam brian s i l ic e o u s rock s sim ilar to th e m arker-bed member and

h a s p roposed that each lam ina rep resen ts a th in v o lc a n ic a sh f a l l . The

b a se o f ea ch lam ina i s marked by abundant ch lo r ite due to th e in it ia l

rapid se t t lin g o f th e a sh f a l l . F iner s iz e d p a r tic le s s e t t le d at a s lo w er

rate and crea ted the graded app earance o f th e b a n d s . A sh -fa ll d e p o s i­

tio n w as presum ably im p osed on a co n tin u o u s ly a ccu m u la tin g , c h e m ic a lly

p rec ip ita ted , s i l ic e o u s ro ck . P u ch elt (1973) reported a c h e m ic a lly pre­

c ip ita te d , iro n -r ich s i l i c a g e l occurring near subm arine fum aroles in the

46

M ed iterran ean . This ten d s to g iv e cred en ce to the m echanism proposed

for the d e p o s it io n o f the m arker-bed m em ber.

D e p o s it io n o f the T u ff-B reccia M em ber

R enew ed v o lc a n ic a c t iv ity w a s marked by the d e p o s it io n o f the

a n d e s it ic tu ff-b r e c c ia member over the m arker-bed m em ber. Perhaps the

m ost strik ing feature o f the tu ff-b r e c c ia unit i s the le n s e s o f c o a r se v o l­

c a n ic b r e cc ia in terbedd ed w ith the tu f f s . T h ese b r e c c ia s are res tr ic ted

to the southern part o f the study area and are thought to be e ith er the re­

su lt o f a s e r ie s o f phreatom agm atic e x p lo s io n s or fragm ents torn from

the v en t w a lls during eruption o f the tu f fs . The g en era l s im ila r ity o f the

texture and co m p o sitio n o f the fragm ents to the e n c lo s in g tu ffs favors

the phreatom agm atic theory o f o r ig in . A w ater-m agm a e x p lo s io n i s th e

assu m ed orig in for the c o a r se v o lc a n ic b r e cc ia s a s s o c ia te d w ith the

m a ss iv e su lfid e d e p o s its o f Kuroko, Japan (Tatsumi and W a ta n a b e ,

1 9 7 1 ). G angster (1972) referred to th is type o f b recc ia a s "m ill-rock"

and noted i t s a lm ost u n iv ersa l p r e se n c e around m a ss iv e su lfid e d e p o s its

in C anad a. The sp a tia l r e s tr ic tio n o f the b r e c c ia s to th e southern part o f

th e stud y area and th e gradual d e c r e a se in fragm ent s iz e to the north

im ply th at the a n d e s it ic magma reach ed the o c e a n floor from a v en t in the

southern part o f the a r ea . C on tact w ith s e a w ater c a u se d th e magma to

exp lod e and resu lted in the d e p o s it io n o f a fa n -sh a p e d b r e cc ia zon e on

the flan k s o f a rh y o lite d o m e . T his p r o c e ss co u ld h ave occurred a num­

ber o f t im e s , a s there are s e v e r a l, s tra tig ra p h ica lly sep a ra te b recc ia

z o n e s .

47

E ffects o f the F irst D eform ation

The structural fabric o f the study area i s dom inated by th o se

e lem en ts crea ted during a major Precam brian te c to n ic e v e n t . This ev en t

produced north- to n orth east-tren d in g fo ld s , fo lia t io n , and rev erse

fa u lts . Lower h em isp h ere p ro jec tio n s o f o r ien ta tio n s o f fo ld a x e s m ea­

sured for th is study (F ig. 27c) d isp la y a unim odal d istr ib u tio n o f p o in ts

as do the p o le s - t o - a x ia l su r fa ces (F ig. 15 ). The strong h om ogen eity o f

fo ld -a x is o r ien ta tio n s im p lie s th at a ll fo ld s w ere crea ted by a s in g le

fo ld ing e v e n t . Fold a x e s th at do not conform w ith the preferred so u th -

so u th w est trend may rep resen t lo c a l v a r ia tio n s in the s tr e s s f ie ld during

> fo ld in g .

E ven sen (1969) h a s in v e s t ig a te d th e m etam orphic fea tu res o f

the rock s o f the study area and h a s a s s ig n e d the rock s to the low er

g r e e n sc h is t f a c ie s . R e cr y sta lliz a tio n o f ch lo r ite in to rod lik e g r a in s ,

w hich are p a r a lle l to fo ld a x e s , s u g g e s ts that m etam orphism w a s c o n ­

tem poraneous w ith fo ld in g . M ost structural e lem en ts o f the stu d y area

are very s im ilar in trend and s ty le to the structural e lem en ts attributed

to the M a za tza l R evolu tion by W ilso n (1962). C o n seq u en tly , it is a s ­

sum ed that th e fir s t deform ation o f the study area c o in c id e d w ith the

M a za tza l R evo lu tion .

E ffec ts o f the Second D eform ation

The seco n d period o f deform ation crea ted s m a ll - s c a le stru ctu res

sim ilar in o r ien ta tio n to th o se crea ted by the f ir s t period o f deform ation .

Structural fea tu res o f the study area that are due to the sec o n d deform a­

tio n are rev erse fa u lts w ith sm all sep a ra tio n , kink fo ld s , and d ia b a se

48

d ik e s . T h ese fea tu res are very sim ilar to the fea tu res attributed by

W ilso n (1962) to the Grand C anyon D is tu rb a n ce . C o n seq u en tly , it i s

assu m ed that the se c o n d deform ation o f the study area c o in c id e d w ith

the Grand C anyon D is tu r b a n ce .

E xperim ental work by D onath (1968) h a s dem onstrated th at kink

fo ld s form in r e sp o n se to co m p ress io n p a ra lle l to or at a low a n g le to

a n istrop ic fea tu res in the rock , su ch a s fo lia t io n . Kink fo ld s o b served

in the m ine w orkings appear to h ave resu lted from the w ed gin g o f b lo c k s

o f rock b etw een tw o fa u lts (F ig. 2 3 ) . Such m ovem ent w ould im p ose a

v e r t ic a l c o m p r e ss iv e force on the nearly v e r t ic a l fo lia t io n to form the

kink f o ld s .

The d ia b a se d ik es are a s s ig n e d to th is sec o n d period o f defor­

m ation b e c a u se o f th eir reco g n ized a s s o c ia t io n with th is e v en t (W ilson ,

19 6 2 ). No radiom etric age determ inations h ave b een made on the d ia ­

b a se d ik es o f the stu d y a rea .

E vidence for p ost-P recam b rian stru ctu res w a s not found in the

study a rea . The c o n s is t e n t unim odal symmetry o f the structural fabric

data (F ig s . 12 , 13 , 14 , 15, and 2 7c) strongly im p lie s th at there h a s

b een o n ly on e period o f major deform ation in th e stud y a rea . All s tru c­

tures o b serv ed are c o n s is t e n t w ith the s ty le and or ien ta tio n o f stru ctu res

ascr ib ed to Precam brian te c to n ic e v e n t s . Laramide in tru sio n s are not

reco g n ized in the im m ediate area , and B asin -a n d -R a n g e fau ltin g d o e s

not seem to h av e a ffec ted th e a rea .

49

K inem atic M odel for Structural H istory

The fabric data gath ered during f ie ld work perm it the d e v e lo p ­

ment o f the fo llo w in g k in em atic m odel for th e structural h is to ry o f the

study area . C om p ression in an e a s t - w e s t d irectio n in it ia te d fo ld in g in

the th ick seq u en ce o f v o lc a n ic and sed im entary rock s and crea ted g e n tle

fo ld s h av in g a n orth -sou th a x ia l tren d . I n it ia l ly , the fo ld in g w a s accom ­

p lish ed by a f le x u r a l-s lip m echanism in w hich rock la y ers s l id over each

other a long bedding p la n e s (Donath and Parker, 1 9 6 4 ). Folding con tin u ed

u n til tig h t fo ld s w ere formed and ad d ition a l co m p ress io n co u ld not be a c ­

com m odated by flexu ra l s l ip . F o lia tio n d ev e lo p ed at th is tim e, and c o n ­

tinued s tr e s s on th e rock s c a u se d tra n sp o s itio n to o ccu r a long fo lia t io n

p la n e s . As a r e su lt , i s o c l in a l sim ilar fo ld s w ere c r e a te d . B eca u se b ed ­

ding w a s not an a c tiv e e lem en t during the la ter s ta g e s o f th is fo ld in g

e v en t, the fo ld in g m echanism i s d es ig n a ted a s p a s s iv e s l ip (Donath and

Parker, 1 9 6 4 ). Ramsay (1967 , p . 430) v ie w s p a s s iv e s lip a s "the on ly

m echanism th at h a s b een su g g e s te d to ex p la in s a t is fa c to r ily the g e o ­

m etrica l form o f p er fec t sim ilar fo ld s . . . "

Further c o m p ress io n c a u se d fracturing o f the rock and th e forma­

tion o f s te e p ly d ipping rev erse fa u lts , w hich are , in g e n e r a l, p a r a lle l to

fo lia t io n . This typ e o f fau lt i s w e ll e x p o sed in th e m ine w orkings and

forms th e fo o tw a ll c o n ta c t o f the ore zon e on the 300 and 400 le v e l s

(F ig. 2 ) .

The form ation o f the Shylock fau lt zon e i s p o s s ib ly a la te fe a ­

ture o f the fir st deform ation . The fa u lt c r o s s e s fo lia t io n and fo ld s and

h as a c o n s is t e n t le ft-h a n d ed s e n s e o f sep a ra tio n . The fa u lt i s intruded

50

by d ia b a se d ik es a s s o c ia te d with the seco n d period o f deform ation , in ­

d ica tin g the fa u lt's e x is t e n c e a t the tim e o f in tru sio n .

The p a r a lle l o r ien ta tio n o f structural fea tu res attributed to both

p eriod s o f deform ation im p lie s a s im ila r ly orien ted s tr e s s f ie ld for both

e v e n t s . W h ereas the rock s deform ed p la s t ic a l ly during m ost o f the fir s t

p er io d , th ey c o n s is t e n t ly deform ed in a b rittle manner during the sec o n d

p eriod . The brittle behavior r e f le c ts a d e c r e a se in co n fin in g p ressu re

and probably in tem perature o f the rock s during the seco n d e v e n t .

SULFIDE HISTORY

A p r e c ise understanding o f the age r e la t io n sh ip s o f the su lfid e

m inerals w ith th eir e n c lo s in g rock s i s im perative to an ev a lu a tio n o f the

mode o f or ig in o f su lfid e m in era liza tio n at the C opper Q u een m in e. Struc­

tural and tex tu ra l data are u t il iz e d to interpret the deform ation and d e p o -

s it io n a l h is to ry o f the su lfid e m in e r a ls .

D eform ation o f the S u lfid e -r ich Bands

The su lf id e -r ic h bands e x h ib it fo ld s s im ilar in s ty le and o r ien ­

ta tion to the fo ld s ex h ib ited by the e n c lo s in g m arker-bed m em ber. F ig ­

ures 27b and 27c show the s t a t is t ic a l h om ogen eity o f fo ld -a x is

o r ien ta tio n s for fo ld s in the su lf id e -r ic h bands and a ll fo ld s m easured

in the stud y a rea . This h om ogen eity o f fabric c le a r ly d em on strates th at

the su lf id e -r ic h bands and the e n c lo s in g rock h a v e undergone id e n t ic a l

deform ational h is t o r ie s . This n e c e s s i t a t e s th at th e su lf id e -r ic h bands

w ere p resen t in the m arker-bed member prior to the fir st period o f defor­

m ation . Figure 28 sh o w s a fragm ent o f a su lf id e -r ic h band w h ich i s now

d iscord an t w ith fo lia t io n . This re la tio n sh ip a ls o req u ires o f su lfid e

m in erals a s bands in th e m arker-bed member prior to deform ation .

O rigin o f the S u lfid e M in era liza tio n

T h eories on the orig in o f the su lfid e m in era liza tio n in th e C op­

per Q ueen m ine area m ust e f fe c t ly in tegrate structural and c h e m ic a l data

to d ev e lo p a ten a b le p o s it io n . A pre-d eform ation age for th e su lfid e m in­

era liza tio n ca n be s a t is f ie d by e ith er a sy n g e n e t ic or e p ig e n e t ic o r ig in .

51

52

Figure 28. Fragment of lam inated su lfide-rich band exposed on 400 level

Fragment h as been ro tated and is now d iscordan t with fo lia tion .

53

H o w ever , in trod uction o f su lfid e m in erals in to an e x is t in g rock

by a hydrotherm al rep lacem en t p r o c e ss m ight h ave resu lted in a reco g ­

n iza b le p a ra g en etic seq u e n c e o f su lfid e m ineral d e p o s it io n . T ex tu res ,

such a s c u sp s and c a r ie s th at w ould be ex p ec ted in a se q u e n tia lly d e ­

p o s ite d , hydrotherm al su lfid e a ssem b la g e o f rep lacem en t o r ig in , are

g en era lly a b sen t in sp ec im en s from th e C opper Q u een m in e . The su lfid e

m in erals occu r a s lam inated b a n d s , w hich are c o n s is t e n t ly p a r a lle l to

bedding in the e n c lo s in g rock . An e p ig e n e t ic rep lacem en t or ig in for the

bands w ould require extrem e s e le c t iv i t y in the rep lacem en t p r o c e s s .

The la ck o f fea tu res ty p ic a lly c a lle d upon to dem onstrate hydrotherm al

rep lacem en t o r ig in , such a s a reco g n iza b le ig n eo u s sou rce for th e m in­

e ra liza tio n and the p r e se n c e o f m in era liz in g c h a n n e ls , m akes an e p i­

g e n e t ic or ig in for the su lfid e m in era liza tio n u n attractive to th e w r iter .

M in era liza tio n i s thought to be th e r e su lt o f su lfid e m in era ls

p rec ip ita tin g from s e a w ater due to em anations o f b a se m eta ls and su l­

fur from fum arolic v e n t s . H onnorez e t a l . (1973) h ave reported on the

subm arine d e p o s it io n o f iron su lfid e from fum arolic v e n ts near S ic i ly .

They o b serv ed th ou san d s o f bubbling fum aroles on the flan k s o f a re­

c e n tly a c t iv e is la n d -a r c v o lca n o d e p o s it in g p yrite and marc a s ite on the

s e a flo o r . Their (1973 , p . 160) v ie w s con cern in g the ro le o f fum aroles

and the sou rce o f the m eta ls are:

The fum aroles provide the s e a w ater w ith an un lim ited su p p ly o f H 2 S and h e a t , and the low pH w hich i s required; an e x c e s s o f c o llo id a l S resu ltin g from HgO o x id a tio n (by th e O2 d i s ­so lv e d in s e a water) i s g en era lly kept in su sp e n s io n w here the su lfid a tio n rea c tio n s o c c u r . . . . It i s r ea so n a b le to think th at th e major parts o f the com p on en ts o f fum arolian d e p o s it s , and among them th e m e ta llic e lem en ts su ch a s F e , are due to pre­c ip ita t io n o f r e c y c le d com p on en ts from the country r o c k s , th e v o lc a n ic p ile and the c ru sta l rock s o f th e b a sem en t.

They (1973 , p . 167) further d e scr ib e the d e p o s it io n a l products o f the

fum aroles a s fo llo w s:

T h ese a ltern a tio n s o f d e c im e te r -th ic k m in era lized le v e ls w ith th ick er barren la y e r s , a s w e ll a s abrupt c h a n g e s in su lfid e co n ten t or the gradual z o n e s o f d iffu se m in era liza tio n are a l l c h a r a c te r is t ic o f v o lc a n ic sed im en tary su lfid e d e p o s i t s .

The o b v io u s s im ila r it ie s b etw een the su lf id e -r ic h bands at the C opper

Q ueen m ine and th e su lf id e -r ic h bands p resen tly forming in th is s y n -

g e n e t ic sy stem are e s p e c ia l ly str ik in g and add com p ellin g argum ents

for the sy n g e n e tic or ig in o f the C opper Q ueen ore b o d y .

COMPARISON OF THE COPPER QUEEN ORE BODY WITH SIMILAR DEPOSITS

C om parison o f the C opper Q ueen ore body w ith other m a ss iv e

su lfid e d e p o s its thought to be sy n g e n e tic sh o w s many strik ing s im ila r ­

i t i e s . The d e p o s its at Jerom e, A rizona, and N oranda, Q u e b e c , w ere

c h o se n for com p arison b e c a u se o f the s im ila r ity o f th eir g e o lo g ic s e t ­

tin g to th e C opper Q u een d e p o s it .

Jerom e, Arizona

The m a ss iv e su lfid e ore body at Jerome o ccu rs at a r h y o lite -

d a c ite c o n ta c t in Precam brian rock s about 100 m . y . o ld er than th e Big

Bug G roup. The d e p o s it w a s in it ia lly interpreted a s an e p ig e n e t ic re ­

p lacem en t typ e (Lindgren, 1926; A nderson and C r e a se y , 1 9 5 8 ). R ecent

work by A nderson and N ash (1972) h a s perm itted a rein terp reta tion o f

ea rlier d a ta . The d e p o s it i s now d escr ib ed a s a sy n g e n e t ic ore body

formed by hot brin es that w ere d isch a rg ed in to a subm arine b a s in during

d e p o s it io n o f the e n c lo s in g rock . If sy n g e n e tic d e p o s it io n o f s u lf id e s

occurred at Jerome in a d e p o s it io n a l environm ent s im ila r to that o b serv ed

at the C opper Q u een d e p o s it , it w ould not be i l lo g ic a l to a ssu m e the

sam e m echanism o f su lfid e form ation w as a c t iv e in both lo c a l i t i e s .

N oranda, Q u eb ec

The M illen b ach m ine at N oranda, Q u e b e c , i s a b an d ed , m a ss iv e

su lfid e d e p o s it occurring at a r h y o lite -d a c ite c o n ta c t in Precam brian v o l­

c a n ic and tu ffa ceo u s sed im en tary r o c k s . Simmons' (1973 , p . 18)

55

56

d escr ip tio n o f the form ation o f the d e p o s it favors a sy n g e n e tic or ig in for

the su lfid e m in era liza tio n . (QFP = q u a rtz-fe ld sp a r-p o rp h y ry .)

C o in c id en t w ith the d e p o s it io n o f another tu ff la y er (the "Inter-QFP T uff"), m eta l-b ea r in g hydrotherm al so lu tio n s approached su rface co n tro lled by the v en t r e sp o n s ib le for the recen t QFP and by stru ctu res w ith in the o ld er r o c k s .W ith rapid ch a n g e s in p h y s ic a l and c h em ica l co n d itio n s near su r fa c e , in crea s in g am ounts o f su lp h id e s w ere d e ­p o s ite d in fractures (p o ss ib ly produced by p h reatic e x p lo ­s io n s fo llo w in g QFP extru sion ) and fin a lly a s c o a r s e ly banded m a ss iv e su lp h id e s at su r fa c e .

The c o in c id e n c e o f th e ore zon e w ith the tu ff la y er i s id e n t ic a l to th e

ore zon e-m a rk er-b ed member re la tio n sh ip o b serv ed in th e C opper Q u een

ore b od y .

CONCLUSIONS

The g e o lo g ic h isto ry and interpreted mode o f form ation o f the

C opper Q ueen ore body are d ev e lo p ed from p e tr o lo g ic , petrograp h ic ,

m ineragraphic, and structural data from the study a rea . V olcan ic and

sed im entary rock s o f th e Precam brian Y avapai S er ies w ere d e p o s ite d in

a major g e o sy n c lin e a s th e r esu lt o f v o lc a n ism . E x ten siv e subm arine

fum arolic a c t iv ity near rh yo lite dom es in term itten tly d isch a rg ed b a se

m eta ls and su lfu r in to the s e a , c a u s in g su lfid e m in erals to be d e p o s ite d

a s lam inated bands w ith in a con tem p oran eou sly forming e x h a lit e . D ep o ­

s it io n o f the su lf id e -r ic h bands c e a s e d w ith ren ew ed v o lc a n ic a c t iv ity

and the d e p o s it io n o f a n d e s it ic tu ffs and v o lc a n ic b r e c c ia s . Rocks and

su lfid e m in erals w ere la ter su b jec ted to the fir st deform ation , w hich

crea ted tig h t to is o c l in a l fo ld s and th e p e r s is te n t fo lia t io n o b serv ed in

the study a rea . The sec o n d deform ation crea ted sm all r ev erse fa u lts ,

kink f o ld s , and d ia b a se d ik e s . L ittle e v id e n c e for p ost-P recam b rian

deform ation w as o b se rv e d . The la ck o f fea tu res ty p ic a lly c a lle d upon to

dem onstrate hydrotherm al rep lacem en t m akes an e p ig e n e t ic or ig in for th e

su lfid e m in era liza tio n u n attractive to the w riter . The C opper Q u een d e ­

p o s it i s therefore v ie w ed a s a sy n g e n e t ic a lly formed su lf id e body sim ilar

in or ig in to the ore b o d ies at Jerom e, A rizona, and N oranda, Q u e b e c .

57

REFERENCES

A nderson, C . A ., 1 9 7 2 , Precam brian rock s in the C ordes a rea , Y avapai C ou n ty , Arizona: U .S . G e o l. Survey B u ll. 1345 , 36 p .

A nderson, C . A . , and B la ce t, P . M . , 1 9 7 2 , Precam brian g e o lo g y o f the northern Bradshaw M ou n ta in s, Y avapai C ou n ty , Arizona: U .S . G e o l. Survey B u ll. 1336 , 82 p .

A nderson, C . A ., B la c e t , P . M ., S ilv er , L. T . , and Stern , T. W . ,1971 , R ev is io n o f Precam brian stratigraphy in the P r e sc o tt- Jerome a rea , Y avapai C ou n ty , Arizona: U .S . G e o l. Survey B u ll. 1 3 2 4 -C , 15 p .

A nderson, C . A ., and C r e a se y , S . C . , 1958 , G eo lo g y and ore d e p o s its o f the Jerome area , Y avapai C oun ty , Arizona: U .S . G e o l. Sur­v e y Prof. Paper 3 0 8 , 185 p .

A nderson, C . A ., and N a sh , J. T . , 1 9 7 2 , G eo lo g y o f th e m a ss iv e s u l­fid e d e p o s its o f Jerom e, A rizona— a rein terp retation: E con . G e o l . , v . 6 7 , p . 8 4 5 -8 6 3 .

B la c e t, P . M . , 1 9 6 8 , G e o lo g ic map o f the SE 1/4 M ount U nion quad­ra n g le , Y avapai C ou n ty , Arizona: U .S . G e o l. Survey o p e n - f i le report.

Brook, K ., 1973 , Banded iron form ations o f the M ayer, A rizona area and th eir a p p lica tio n to m ineral exp loration : private report to C om inco Am erican I n c . , T u cson , A rizona.

D on ath , F . , 1968 , E xperim ental stud y o f k in k -b an d d eve lop m en t in M artinsburg s la t e , jn P roceed in gs o f the C on feren ce on R esearch in T e c to n ic s , Baer, A. J . , and N orris , D . K. ( e d s .) : C anada G e o l. Survey paper 6 8 -5 2 .

D on ath , F . , and Parker, D . , 1964 , F o ld s and fo ld in g: G e o l. S o c . Am erica B u l l . , v . 75 , p . 4 5 -6 2 .

D o u g la s , S . , 1 9 5 6 , C opper Q u een m in e, Big Bug d is tr ic t , Y avapaiC ou n ty , Arizona: Arizona D e p t, o f M ineral R e so u r c es , P h oen ix , o p e n - f i le r e p t . , 2 p .

E v en sen , J. M . , 1969 , G eo lo g y o f th e cen tra l portion o f th e Agua Fria m ining d is tr ic t , Y avapai C oun ty , Arizona: unpubl. P h .D . d i s ­ser ta tio n , U n iv ersity o f A rizona, 121 p .

F leu ty , M . J . , 1 9 6 4 , The d e scr ip tio n o f fo ld s: G e o l. S o c . Am erica P ro c . , v . 75 , p . 4 6 1 -4 9 2 .

58

59

G r o ss , C . A . , 1 9 6 5 , G eo lo g y o f iron d e p o s its in C anad a, G eneralg e o lo g y and ev a lu a tio n o f iron d e p o s it s , V ol. 1: C anada G e o l. Survey, B oon. G eo lo g y Kept. 2 2 , 181 p .

H onn orez, J . , H o n n o rez -G u erste in , B . , V a le tte , J . , and W auschku h,A ., 1 9 7 3 , P resen t day form ation o f an e x h a la tiv e su lfid e d e ­p o s it at Vulcano (Thyrrhenian S e a ) , Part II. A ctive c r y s ta l l iz a ­tio n o f fum arolic s u lf id e s in the v o lc a n ic sed im en ts o f the Bala di L evan te , In O res in sed im en ts: B erlin , Springer-V erlag, p . 1 3 9 -1 6 6 .

H u d lesto n , R. J . , 1973 , Fold m orphology and som e g eo m etr ica l im p lica ­tio n s o f th eo r ie s o f fo ld developm ent: T e c to n o p h y s ic s , v . 1 6 , p . 1 -4 6 .

Jaggar, J . A . , and P a la ch e , C . , 1 9 0 5 , D escr ip tio n o f Bradshaw M oun­ta in s qu adrangle , Arizona: U .S . G e o l. Survey A tlas fo lio 126 ,11 p .

Jam es, H . C . , 1954 , Sedim entary fa c ie s o f iron form ations: E con . G e o l . , v . 4 9 , p . 2 3 5 -2 9 3 .

L avery, N . G . , 1972 , Graded v o lc a n ic a sh -c h e r t b e d s— a u se fu l in d ic a ­tor o f stratigrap h ic or ien ta tio n in Archean v o lc a n ic rocks:E con . G e o l . , v . 6 7 , p . 1 1 1 -1 1 2 .

Lindgren, W . , 1926 , Ore d e p o s its o f the Jerome and Bradshaw M oun­ta in s q u ad ran g les, Arizona: U .S . G e o l. Survey B u ll. 7 8 2 ,192 p .

P u ch elt, H . , 1973 , R ecent iron sed im en t form ation at the Kameni I s la n d s , Santorin (G r e ec e ), in O res in sed im en ts: B erlin , Springer- V erlag, p . 2 2 7 -2 4 6 .

R am say, J. G . , 1967 , Fold ing and fracturing o f rock s: New York, M cG raw -H ill Book C o . , 568 p .

R idler, R. H . , 1973 , E xhalite co n cep t: a new to o l for exp loration : The Northern M iner (N ov. 2 9 ) , p . 5 9 -6 0 .

Sander, B . , 1 9 3 0 , G efugekunde der G e ste in e : B erlin , Springer.

S a n g ster , D . F . , 1972 , Precam brian v o lc a n o g e n ic m a ss iv e su lp h id e d e ­p o s it s in C anada: a rev iew : C anada G e o l. Survey paper 7 2 -2 2 , 44 p .

S ch u ch ert, C . , 1923 , S ite s and nature o f the North Am erican g e o sy n ­c l in e s : G e o l. S o c . Am erica B u l l . , v . 3 4 , p . 1 5 1 -2 3 0 .

Sim m ons, B. D . , 1973 , G eo lo g y o f the M illen b ach m a ss iv e su lp h id e d e p o s it , N oranda, Q u eb ec , C anada: paper p resen ted to the 75th Annual G en era l M eetin g o f th e C IM , V ancouver, B .D .

60

T atsum i, T . , and W atan ab e , T . , 1971 , G e o lo g ic a l environm ent o f for­m ation o f the K uroko-type d e p o s its : S o c . M in . G e o l. Japan, S p e c . I s s u e 3 , p . 2 1 6 -2 2 0 .

Turner, F . J . , and W e is s , L. E . , 1963 , Structural a n a ly s is o f m etam or- p h ic te c to n ite s : N ew York, M cG raw -H ill Book C o . , 545 p .

U ytenbogaardt, W . , and Burke, E. A. J . , 1 9 7 1 , T ab les for m icro sco p ic id e n t if ic a tio n o f ore m inerals: New York, E lsev ier P u b lish in g C o . , 430 p .

W ilso n , E . D . , 1 9 3 9 , Pre-C am brian M a za tza l rev o lu tio n in cen tra l Arizona: G e o l. S o c . Am erica B u l l . , v . 5 0 , p . 1 1 1 3 -1 1 6 4 .

W ils o n , E. D . , 1 9 6 2 , A r^sumd o f th e g e o lo g y o f Arizona: Arizona k Bureau o f M in es B u ll. 17 1 , 140 p .

0 1 63 9 ^ . ^ '

zSP/O// 9 7 < /3&5

o2 m a p ^

DIAB.

EXPLANATION

DIABASE DIKES

QUARTZ VEINS

T U F F - B R E C C I A MEMBER INTERBEDDED, ANDESITIC

TUFFS AND BRECCIAS

MARKER-BED MEMBER ----- LAMINATED, GREEN, TUFFACEOUS

SEDIMENTS; ORE ZONE INDICATED BY STIPPLED PATTERN

RHYOLITE-DACITE MEMBER WHITE AND PURPLE

VOLCANICS WITH QUARTZ PHENOCRYSTS

-d-60

^ 3 2

SYMBOLS

STRIKE AND DIP OF BEDDING

STRIKE AND DIP OF OVERTURNED BEDDING

STRIKE AND DIP OF FOLIATION

FOLIATION WITH TREND AND PLUNGE OF LINEATION

TRACE AND DIP OF AXIAL SURFACE WITH TREND AND PLUNGE OF FOLD AXIS

/

CONTACT WITH DIP DASHED WHERE INFERRED

FAULT WITH DIP, SHOWING RELATIVE MOVEMENT — DASHED WHERE INFERRED

CLOSELY SPACED FRACTURES

RAISE OR WINZE

APPROXIMATE MEAN DECLINATION

FIGURE 2

GEOLOGIC MAP

OF THE

3 0 0 a 4 0 0 LEVELS

COPPER QUEEN MINE

YAVAPAI COUNTY, ARIZONA

4 0 0 level portal

D.K.BROOK,JR, M S. THESIS,DEPARTMENT OF GEOSCIENCES, 1974

£ 7 7 9 /19793fc5"

D.K.BROOK,JR.,M.S. THESIS,DEPARTMENT OF GEOSCIENCES, 1974

£W !m i