GEOLOGICAL SURVEY CIRCULAR 614 

Metalliferous Deposits 

Near Granite Mountain 

Eastern Seward Peninsula 

Alaska 

Metalliferous Deposits 

Near Granite Mountain 

Eastern Seward Peninsula 

Alaska 

By Thomas P. Miller and Raymond l. Elliott 

GEOLOGICAL SURVEY CIRCULAR 614 

Washington 1969 
United States Department of the Interior 

WALTER J. HICKEL, Secretary 

Geological Survey 

William T. Pecora, Director 

Free on application to the U.S. Geological Survey, Washington, D.C. 20242 
CONTENTS 

Page Page 

Abstract -----------------------------------

Introduction --------------------------------

Geologic setting -----------------------------

~ineral deposits ----------------------------

1 

1 

5 

6 

6 

Mineral deposits-Continued 

Upper Peace River ______________________ 12 

Bear Creek ----------------------------- 14 

Summary ----------------------------------- 14 

Quartz Creek --------------------------- References cited ----------------------------- 14 

FIGURE 1. 

2. 

3-6. 

7. 

8. 

TABLES 1-2. 

3. 

4. 

ILLUSTRATIONS 

Geologic map of the Granite Mountain region showing location of areas described in tex"; __ 

Geologic map of the Quartz Creek area -----------------------------------------------

~aps of the Quartz Creek area showingS. Lead distribution in stream sediments ---------------------------------------

Page 

2 

4 

8 

4. Zinc distribution in stream sediments --------------------------------------- 9 

5. Copper distribution in stream sediments ------------------------------------- 10 

6. Boron distribution in stream sediments -.,------------------------------------

Geologic map of the upper Peace River area -----------------------------------------

Map showing location of stream-sediment samples of the upper Peace River area _______ _ 

TABLES 

Analyses of bedrock and soil samples from1. Quartz Creek area -----------------------------------------------------------

2. Upper Peace River area -------~---------------------------------------------­

Analyses of stream-sediment samples from the upper Peace River area ----------------

Analyses of selected grab samples from the Bear Creek prospect ------------------------

III 

11 

13 

13 

Page 

16 

18 

19 

19 

METALLIFEROUS DEPOSITS NEAR GRANITE MOUNTAIN 

EASTERN SEWARD PENINSULA, ALASKA 

By THOMAS P. MILLER and RAYMOND L. ELLIOTT 

ABSTRACT 

New deposits of lead, zinc, and silver were found in a 

large altered zone 18 miles long and 2 to 5 miles wide 

near Quartz Creek west of Granite Mountain in the 

eastern Seward Peninsula, Alaska. New deposits of 

molybdenum, 'bismuth, and silver were found associated with a previously reported occurrence of uranium, 

copper, lead, and zinc minerals in the upper Peace 

River drainage northeast of Granite Mountain. Both 

groups of deposits are associated spatially with felsic 

plutonic rocks and occur near the western edge of a 

late Mesozeic province of volcanic plutonic rocks. Both 

groups of deposits warrant further investigation as 

possible exploration target areas. 

INTRODUCTION 

New deposits of lead, zinc, and silver were 

found over a large mineralized area near Quartz 

Creek west of Granite Mountain, in the eastern 

Seward Peninsula, Alaska, during investigations conducted in 1968 as part of the U.S. Geological Survey's Heavy Metals program. In 

addition, anomalous concentrations of molybdenum, silver, and bismuth were found in 

altered syenite and quartz veins in the upper 

Peace River drainage basin northeast of 

Granite Mountain at a locality where anomalous 

amounts of lead, zinc, copper, and uranium 

have been reported in panned concentrates 

(Gault and others, 1953). A previously known 

lead-zinc-gold deposit at Bear Creek (Herreid, 

1965) was reexamined and sampled. Placer 

gold has been mined on a small scale at several 

localities since the 1900's, and a little platinum 

has been recovered as a byproduct. The area 

has not, however, been extensively prospected 

for other metals. 

The deposits occur in the Candle B-5, B-6, 

C-5, and C-6 quadrangles (mapped at scale of 

1 :63,360). The closest towns are Candle, 45 

1 

miles northeast; Buckland, 40 miles north; and 

Koyuk, 40 miles south. At Bear Cre~k a small 

dirt landing field suitable for light aircraft was 

in use during the summer of 1968. Another 

landing strip along the South Fork of Quartz 

Creek has apparently been unused for many 

years, but small balloon-tired aircr2ft may be 

able to land in the east-west directic"'l (fig. 1). 

The landing field at the microwave relay station 

at Granite Mountain itself is restricted and 

unavailable for civilian use. Most of the area 

is tundra covered and free of brush except 

locally along major stream bottoms. The area 

is one of moderate relief comprised of flattopped mountains and ridges up to 2,800 feet 

in altitude that form the divide between the 

Kiwalik and Buckland Rivers. 

More than 400 rock, stream-sediment, and 

soil samples collected during the study of the 

Granite Mountain region were analyzed by 

semiquantitative spectrographic and atomicabsorption methods; results were: available 

while fieldwork progressed. A helicopter was 

used throughout the investigation of the 

Granite Mountain region-an investigation 

which lasted about 3 weeks during the summer 

of 1968. 

The authors were ably assisted in the field by 

Donald H. Grybeck and Richard F. Hardyman, 

geologic field assistants ; Grybeck also assisted 

in the polished-section study. Semiquantitative 

spectrographic analyses were done by K. J. 

Curry, E. E. Martinez, and J. M. Motooka, and 

atomic-absorption analyses were done by R. L. 

Miller and W. R. Vaughn. Officials of the Radio 

Corp. of America and their personnel at the 

Granite Mountain microwave relay station were 

very helpful and cooperative. 
Base from U.S. Geological Survey 

1:250,000 Candle, 1961 

I 

'""" "' 0 

z 

~ 

g: [}

- 20" :r 

..-

APPROXJMATE MEAN 

DECLINATION, 1969 

2 0 2 

QTb 

/ 

/ QTb (_ 

'"" 

Geology by W. W. Patton Jr., (1967) 

MOcliffed by T. P .- Miller and 

R. L. Elliott, 1968 

4 6 MILES 

FIGURE 1.-Geologic map of the Granite Mountain region showing location 

of areas described in text. 

2 
0 

Floodplain deposits 

Terrace ~ deposits 

B 

Basalt 

G G 

Quartz Monzonite, 

monzonite syenite, and 

nepheline 

syenite 

G 

Andesitic 

volcanic rocks 

0 

Limestone 

and schist 

EXPLANATION 

>-< 

p::, 

<t: 

z 

p::, 

[J..l 

~'-" 

~ a 

...... r ~ >:: ::: ~0""' <t:Z p::, H<l; [J..l 

~'-" ~'-" ~ <t: "-1 ::J 1'-" CY Gr § 

AHEOeJ:'ed E5 

rhyolite 5 

r ~ '-" ::J u 0 HO "-1 ({)Z U ({)<!; <t: <t: ~'-" ~ "-1 ::J ~ 

'J u 

}~ u 

H 

0 

N 

Approximate contact 

Approximate -----fault 

)( 

Bear Creek prospect 

~ 

Mine 

~ 

Abandoned mine 

t 

Airstrip 

FIGURE !.-Continued. 

3 
APPROIIMATE 

;~ MEAN 

OE_CLI~JATION. 1969 

Ot KJv 

Qt 

EXPLANATION 

Floodplain deposits 

Terrace deposits 

B 

Basalt 

GG Altered Quartz Monzonite, 

rhyolite monzonite syenite,and 

nepheline 

syenite 

G Andesitic volcanic rocks 

Limestone and schist 

Approximate contact 

Approximate fault 

Boundary of altered 

zone discussed in text 

xs 

Location of analyzed 

sulfide-bearing 

rock samples 

discussed in table 1 

t:.43 

Location of analyzed 

soil samples discussed 

in table 1 

...,.T 

Thermal spring 

Mine 

Abandoned mine 

... Airstrip 

A 

Area described 

in text 

161.30' 

Qt 

/(, 

/ J 

I L 

~~~~----~------~----~ /Pzl / 

161°15' 

KJv 

KJv 

3 MILES/ (Jr .\ 

~·~~~------------~~----~~ Base from U.S. Geological Survey Geology by W. W. Patton Jr., (1967) 

1:250,000 Candle, 1961 Modified by T. P. Miller and R. L. Elliott, 1968 

FIGURE 2.-Geologic map of the Quartz Creek area. 

4 
The first geological report on the Granite 

Mountain region was by Moffit (1905) who 

briefly described the geology of the BucklandKiwalik divide in his report on the gold placers 

of the Fairhaven district. Smith and Eakin 

(1911) and Harrington (1919) discussed the 

gold and platinum placers at Bear and Sweepstakes Creeks. Gault, Killeen, West, and others 

(1953) found anomalous amounts of uraniumbearing minerals and base-metal sulfides in pan 

concentrates in the upper Peace River drainage. 

Herreid (1965) mapped the geology in the 

vicinity of Bear Creek and took geochemical 

samples throughout the northern part of the 

Granite Mountain region. Patton ( 1967) 

mapped the regional geology of the Candle 

quadrangle at a scale of 1 :250,000. 

GEOLOGIC SETTING 

The Granite Mountain region is underlain 

chiefly by andesitic volcanic rocks of Jurassic(?) 

and Cretaceous age intruded by felsic plutonic 

rocks of diverse composition and by small 

hypabyssal felsic intrusives. Metamorphic rocks 

of Paleozoic and perhaps Precambrian age lie 

to the west of the area. Olivine basalt of late 

Tertiary(?) and Quaternary age occurs in a 

few low-lying areas and caps some ridges. The 

mineral deposits in the area are spatially related to the plutonic rocks and occur in both the 

intrusive rocks and in the surrounding country 

rocks. 

Light-gray massively bedded recrystallized 

limestone and dolomite with subordinate 

amounts of mica schist and phyllite crop out 

only in the southwestern part of the map area 

(fig. 1). This unit has been tentatively assigned 

a middle Paleozoic age by Patton (1967) and is 

the oldest bedrock unit in the Granite Mountain region. It is in fault contact with the 

Mesozoic volcanic rocks. 

The next oldest unit is composed of andesitic 

and trachyandesitic pyroclastic and volcaniclastic rocks intercalated with andesite flows. The 

bulk of the unit is thought to be of earliest 

Cretaceous age on the basis of fossil and radiometric age determinations (Patton, 1967). The 

andesite near the contact of the various plutons 

is thermally metamorphosed into rocks of the 

hornblende hornfels facies, and these grade into 

5 

rocks of the albite-epidote hornfels facies away 

from the contact. 

The andesitic volcanic rocks were intruded 

in mid-Cretaceous time by felsic plutonic rocks 

of diverse composition. The Granite Mountain 

pluton is the largest intrusive body in the map 

area. It covers about 30 square miles and is 

roughly circular in plan. The pluton consists 

of a complex composed of a core of h0rnblendepyroxene syenite and monzonite and a border of 

pseudoleucite syenite, biotite pyroxenite, and 

various types of garnet-bearing nepheline syenite. It has been assigned a mid-Cretaceous age 

as a result of a lead-alpha age determination of 

100± 15 m.y. (million years) (Patton, 1967). 

Satellitic stocks of syenite and nepl1~line syenite occur northeast and south of the pluton. 

A hook-shaped pluton, herein called the Quartz 

Creek pluton, of fine-grained biotite-1'0rnblende 

quartz monzonite crops out along the upper 

reaches of the Kiwalik River and Quartz Creek 

(figs. 1 and 2). The northeastern part of the 

pluton is extensively altered. All these bodies, 

though of diverse composition, are tentatively 

correlated_ with nearby plutons to the north 

and northeast that range in composition from 

quartz monzonite to syenite and monzonite and 

that include scattered nepheline syenite complexes (Patton and Miller, 1968; Fatton and 

others, 1968). The plutons in this part of westcentral Alaska have been assigned to the "older" 

suite of Cretaceous plutonic rocks 2.s a result 

of several potassium-argon age determinations 

ranging from 100 to 107 m.y. OtTiller and 

others, 1966). 

Fine-grained dikes (not shown in figs. 1 

and 2), ranging in composition from latite to 

trachyte, and dikes of pseudoleucite porphyry 

cut the andesitic volcanic rocks near the plutons. 

These dikes are generally less than a few tens 

of feet thick. The dikes near the Quartz Creek 

pluton are locally mineralized and contain disseminated pyrite, galena, and sphalerite. 

A small body of intensely altered ard oxidized 

rhyolite intrudes the andesite northwest of 

Granite Mountain (figs. 1 and 2, map unit Kr). 

The rhyolite is tentatively assignee, a Cretaceous age, but its absolute age is unknown. 

Similar rhyolite bodies to the northeast in the 

Shungnak quadrangle are assigned an early 

Late Cretaceous age on the basis cf geologic 
relationships and potassium-argon age determinations (Patton and others, 1968). 

The youngest rocks in the region are the 

vesicular olivine basalt flows of late Tertiary(?) 

and Quaternary age. These flows cover large 

areas of the Kiwalik River valley and cap some 

of the ridges north of Bear Creek. 

The region has not been glaciated, and thus 

the valleys are free of glacial drift. Outcrops 

are sparse owing to the extensive frost riving 

which has reduced most of the exposures to 

rubble. 

The Granite Mountain region is located near 

the west edge of a late Mesozoic province of 

andesitic volcanic rocks and felsic plutonic intrusives. Rocks of this volcanic-plutonic province crop out over much of west-central Alaska 

and the easternmost Seward Peninsula. The 

central and western Seward Peninsula consists 

of a thrust-faulted province of metamorphic 

and sedimentary rocks of Paleozoic age (some 

of these rocks are perhaps as old as Precambrian) cut by intrusive bodies of various compositions. and ages. A north-south boundary 

separates these two provinces. This boundary 

is concealed over much of its length by Quaternary flows, but wherever Mesozoic volcanic 

rocks can be observed in juxtaposition with 

older rocks, the contact is a faulted one. This 

boundary between two provinces so different in 

lithology, age, and tectonic history may be a 

fault over its entire length. 

MINERAL DEPOSITS 

The known mineral occurrences of the 

Granite Mountain region include lead, zinc, 

and silver deposits in the Quartz Creek area; 

a molybdenum, bismuth, silver, copper, lead, 

and uranium deposit in the upper Peace River 

drainage; and a lead, zinc, and gold deposit at 

Bear Creek. The relationships among the individual deposits are unknown, and there are 

differences in mineralogy, chemistry, and lithology. All the deposits, however, are related 

spatially to felsic plutonic rocks. 

Each of the deposits is described in the following sections of the report, and geologic maps 

of the Quartz Creek and upper Peace River 

areas are included. Geochemical maps showing 

the distribution of lead, zinc, copper, and boron 

in stream sediments from the Quartz Creek 

6 

and upper Kiwalik River drainage basins are 

included. These elements were dekrmined by 

semiquantitative spectrographic analyses in 

which the results are reported to the nearest 

number in the series 1, 0.7, 0.5, 0.3, 0.2, 0.15, 

0.1, and so forth. Stream-sediment values of 

70 ppm (parts per million) or greater for lead 

and boron, 100 ppm or greater for copper, and 

10 ppm or greater for molybdenurr" are considered anomalous. Because of the high limit of 

detection for zinc (200 ppm), even detectable 

zinc is considered anomalous. The s~lection of 

these limits is subjective and interpretive on 

the part of the authors ; they are, however, 

based on the distribution of elements in several 

hundred stream-sediment samples collected 

from this geologic province over a period of 

several years. 

Semiquantitative spectrographic and atomicabsorption analyses of mineralized ro~k samples 

are shown in tables 1, 2, and 4. Anomalous 

limits for bedrock samples are difficult to determine, because many of the rock samples are so 

altered that it is impossible to ido.ntify the 

originaf rock or mineral. For this reason, limits 

have been arbitrarily selected for eac:h element. 

These limits, which are thought to be above 

what is generally considered background for 

the various rock types found in tl'~ Granite 

Mountain region, are given at the bottom of 

each table as are the limits of detection of the 

analytical technique. 

QUARTZ CREEK 

Numerous occurrences of arg~ntiferous 

galena, sphalerite, pyrite, and ar;;o~nopyrite 

have been found in an altered zone about 18 

miles long and 2 to 5 miles wide west of Granite 

Mountain (fig. 2). This zone exten1s N. 15° 

W. across the drainage basins of the upper 

Kiwalik River and Quartz Creek and is roughly 

parallel to prominent lineaments in the area. 

Conspicuous reddish-orange oxidized areas and 

large buff carbonate replacement boiies occur 

in the andesite and in the quartz monzonite 

that underlies this zone. A striking feature of 

the mineralized rock in this zone is tl'~ association of sulfides with tourmaline. 

Semiquantitative spectrographic analyses of 

sulfide-bearing material from this zone (table 

1) show, in addition to the high lead, zinc, 

arsenic, and silver contents, consistently high 
boron contents which indicate the abundance of 

tourmaline. The manganese and scandium content is also high. Copper and antimony, though 

present in anomalous amounts in many samples, 

never exceed 2,000 and 700 ppm, respectively. 

Gold is low, less than 1 ppm, even though 

arsenic is high. Tin occurs in about 50 percent 

of the analyzed samples in amounts ranging 

from just detectable to 500 ppm. Many of these 

chemical characteristics are similar to those 

described by Sainsbury and Hamilton (1967) 

as being typical of lode tin deposits. The sulfide 

mineral suite and the abundance of tourmaline 

are also similar to the mineral assemblage of 

the western Seward Peninsula tin district 

(Sainsbury, 1964). 

Many stream-sediment samples from this 

zone contain very anomalous amounts of lead, 

zinc, copper, and boron (figs. 3-6). Silver is 

reported in many of the samples but is never 

more than 0. 7 ppm. Arsenic is reported in some 

samples, particularly near the head of the 

easternmost creek 'in area A where values as 

high as 2,000 ppm occur. Sediment samples 

from streams draining area A contain as much 

as 1,000 ppm lead and 1,500 ppm zinc (figs. 3 

and 4), in addition to anomalous boron and 

copper. Sediment in streams from area C contains anomalous zinc values ranging from 300 

to 1,500 ppm (fig. 4). This low area is completely covered with tundra, and the source of 

the anomaly was not found. Anomalous concentrations of lead, zinc, arsenic, silver, and 

boron were found in soil and rock samples from 

the ridge in area B in the upper Kiwalik River 

drainage (fig. 2). Stream sediments west of 

this ridge (figs. 3 and 4) show anomalous lead 

and zinc. A copper anomaly occurs in the 

stream sediments of the northern part of the 

Quartz Creek drainage basin. The higher copper 

content generally coincides with lower lead and 

zinc values and suggests lateral zonation in the 

major altered zone. The eastern edge of the 

copper anomaly begins in the North Fork of 

Quartz Creek near a small body of intensely 

oxidized rhyolite (map unit Kr, fig. 2; fig. 5), 

and composite grab and soil samples of the 

rhyolite (samples 14, 15, and 16 in table 1) 

show anomalous concentrations of copper, antimony, and boron. The copper anomaly persists 

7 

in the stream sediments of Quartz Creek all the 

way to the Kiwalik River Valley (fig. 2). 

The largest area of sulfidized rock vrithin this 

altered zone is in area A in and around hydrothermally altered quartz monzonite of the 

Quartz Creek pluton (fig. 2). The presence of 

sulfide-tourmaline-quartz-carbonate float in all 

the_ streams draining this -tundra-covered area 

and the location of lode occurrences of sulfide 

minerals and of anomalous stream-sediment 

and soil samples (fig. 2; table 1) outline a 

strongly mineralized area of about 6 square 

miles extending from the ridge at the headwaters of the streams draining area A to about 

a mile north of their junction with the South 

Fork of Quartz Creek. 

The principal sulfide minerals in area A are 

galena, sphalerite, pyrite, and arsenopyrite. 

Realgar and orpiment were found on fracture 

surfaces at locality 28 (fig. 2), and ctalcopyrite 

occurs as small blebs generally associated with 

sphalerite and visible only in polished section. 

The intrusive rock in this area appears to have 

been tourmalinized along closely sp~ced fractures and (or) joints. Where the tourmaline, a 

black to green variety, first replaced the mafic 

minerals, a "bleached" quartz-feldspar-tourmaline rock resulted. Where tourmalinization was 

complete, a dense fine-grained black rock composed entirely of quartz and tourmaline was 

formed. Sericitization has also taken place, 

and where the feldspars were not r~~placed by 

tourmaline, they were sericitized. Late carbonate veins and replacement bodies cut the 

altered quartz monzonite. The andedte in this 

area is also pervasively altered, and scapolite 

is common as thin veinlets and as pseudomorphs after feldspar. The sulfide minerals 

occur in both the altered tourmalinized rock 

and in the carbonate veins as disseminated 

grains, masses, and aggregates of grains. The 

poor exposures and extensive frost riving prohibit determination of the thickness and attitude of the sulfide-bearing material. However, 

at locality 25 (fig. 2), a strongly nineralized 

aggregate of quartz, tourmaline, carl'·:mate, and 

sulfide minerals crops out for about 50 feet in 

the streambed and cutbank. A composite grab 

sample (sample 25B, table 1) shows over 2 percent .lead, 4 percent zinc, and 11;2 ounce per 

ton silver. 
APPRO~IMATE MEAN 

DECLINATION, 1969 

EXPLANATION 

Sample localities showing 

lead concentration in 

parts per million 

0 <70 

<I 70-150 

() 200-500 

• 7[10-1000 

A Area described 

in text 

0 2 

161 °30' 161 '15' 

f------

3 MILES 

I 

J 

FIGURE 3.-Lead distribution in stream sediments of the Quartz Creek area. 

8 
l 

(_ 

f 

~ 

APPRQ,\IMATE MEAN 

[1ECLINATION, 1969 

EXPLANATION 

Sample localities showing 

zinc concentration in 

pa~ts per million 

0 Not detected 

(j Present but <200 

() 200-300 

• 500-1500 

0 

161 "30' 

3 MILES 

I 

! 

FIGURE 4.-Zinc distribution in stream sediments of the Quartz Creek area. 

9 
65"30' 

APPROXIMATE MEAN 

DECLINATION, 1969 

EXPLANATION 

Sample localities showing 

concentration in 

per milliDn 

0 <70 

<I 70 

() 100-150 

• 200-300 

0 

FIGURE 5.-Copper distribution in stream sediments of the Quartz Creek area. 

10 
2: 

~,~-<~ G 

~ f 

~ 

APPROXIMATE MEAN 

DECLINATION, 1969 

EXPl.ANATION 

Sample localities showing 

boron concentration in 

parts per million 

0 <70 

<i 70-200 

() 300-700 

• 1000-2000 

A Area described 

in text 

0 

0 

;.~ /-~'~ 

' I \_/ 

<i 

/ 

FIGURE 6.-Boron distribution in stream sediments of the Quartz Creek area. 

11 
The hooked shape of the Quartz Creek pluton 

suggests the exposed roof of an otherwise concealed pluton. If so, the strongly mineralized 

zone described here may be only part of a larger 

zone along the roof of this pluton. Widespread 

mineralization is also indicated in the andesite 

away from the Quartz Creek pluton throughout 

the 18-mile-long altered zone, as shown by the 

many occurrences of galena, sphalerite, arsenopyrite, and pyrite. These sulfides occur with 

tourmaline as disseminated grains in oxidized 

carbonate veins and replacement bodies. Other 

occurrences of sulfide minerals undoubtedly 

exist in oxidized areas that were not examined 

but are common throughout the large altered 

zone. The original sulfides have been completely oxidized in many cases, but analyses of 

oxidized rock and soil show anomalous lead, 

zinc, silver, arsenic, and boron. Scheelite was 

found in pyrite-tourmaline-quartz vein material in frost-riven rubble at locality 36 (fig. 2) 

and a composite grab sample of this material 

(sample 36, table 1) contained more than 

10,000 ppm tungsten. 

The age of the mineralization is not known. 

Both the Quartz Creek quartz monzonite and 

the small rhyolite body (map unit Kr) are mineralized, but their mutual relationship is uncertain. The 18-mile-long altered zone is roughly 

centered around the east limb of the hookshaped Quartz Creek pluton, and the strong 

mineralization in area A occurs chiefly in the 

quartz monzonite of the pluton. These observations suggest that the mineralization is genetically related to the quartz monzonite. A 

possible structural control of mineralization is 

suggested by the rough parallelism of the trend 

of the 18-mile-long altered zone and prominent 

lineaments in the area. 

All these factors make this large 18-milelong altered zone worth further investigation 

as a possible exploration target. Trenching 

and stripping in area A would help define the 

extent and potential of the large area of mineralized rock there. Soil sampling and perhaps 

the use of reconnaissance electrical geophysical 

methods over much of the upper Kiwalik River 

and Quartz Creek drainage basins might locate 

mineralized areas in the andesite and indicate 

good drilling locations. Drilling would certainly be necessary to determine the extent of 

12 

mineralization in the altered n1etalliferous 

rhyolite (map unit Kr). 

UPPER PEACE RIVER 

Anomalously high concentrations of molybdenum, bismuth, silver, copper, and lead are 

found in the soils, stream sediments, and outcrops of the upper Peace River drainage basin 

(figs. 7 and 8). These anomalous metal concentrations occur over an area of about 2 

square miles centered around the two main 

forks of the Peace River. The area is low and 

tundra covered except for a few scattered outcrops and frost-riven rubble along the cutbanks 

of the creeks. 

The area is underlain by a smf.ll satellitic 

stock of the Granite Mountain pluton. The 

stock is composed of several varietie~ of syenite 

-the most common being a pin]-~ mediumgrained, hornblende-biotite variety. A pink, 

fine- to medium-grained, porphyritic syenite 

composed of over 90 percent perthitic feldspar 

and less than 1 percent mafic minerals is also 

common. Garnet-bearing nepheline syenite 

crops out on the south side of the ridge between 

the northern fork of the Peace River and Cub 

Creek and garnet-bearing nepheHne syenite 

float is common in both forks. 

Locally the syenite contains abundant disseminated pyrite cubes, a little visible finegrained molybdenite, and abundant. accessory 

magnetite and purple fluorite. Composite grab 

samples of syenite taken over areas ranging 

from 10 to 100 square feet contain 15 to 200 

ppm molybdenum (samples 2, 3, 6, 8-13, and 

15 in table 2) as well as anomal0usly high 

amounts of bismuth, silver, and copper. Rubble 

of pyrite-quartz material is also abur!fant along 

the cutbanks of both forks; composite grab 

samples of this material contain from a trace 

to more than 2,000 ppm molybdenum as well as 

anomalously high bismuth, silver, f.nd copper 

(samples 4, 5, 7, and 14 in table 2). A canary 

yellow alteration product, abundart in both 

syenite and vein material, has beer identified 

as ferromolybdite from X-ray diffraction patterns. Where the syenite is cut by pyrite-quartz 

veins, the syenite is bleached and ox~ dized, and 

it contains disseminated pyrite and, less commonly, molybdenite. 

In soils from the banks of the northern fork, 

molybdenum contents reach as high as 70 ppm 
65 

27' 

KJv 

30' \ • 

\ .· I \I 

\ 

" \ 

f 

~·· 

-·. \ I r:ms _.· I 

\ r:m~ \ 

I 

l 

\ '/ / " --/ 

1-Jv 

Base from U.S. Geological Survey 

1:63,360 Candle B-5, 1956 

l 0 I I I I I I I I I I 1 

EXPLANATION 

Monzonite, G syenite, and }~ (;:; 

nepheline syenite . [j 

,.;; 

G ~u U)Z 

())<( 

Andesi tic volcanic rocks ~ 

>-:J 

Approximate contact 

8 

X 

Location of analyzed rock 

sample discussed in table 2 

16 

6. 

Location of analyzed soil 

sample discussed in table 2 

Geology by T. P. Miller 

and• R. L. Elliott, 1968 

MILE 

APPROXIMATE M'EAN 

DECLINATION, 1969 

FIGURE 7 .-Geologic map of the upper Peace River area. 

(samples 16-22 in fig. 7 and table 2) ; and in 

stream sediments from this fork and its tributaries, as high as 30 ppm (samples 3-11 in fig. 

8 and table 3). Copper and lead contents are 

also anomalously high in the stream-sediment 

samples from this area (fig. 8; table 3) ; however, the highest contents of copper and lead 

are in the upper parts of southern and northern 

forks respectively, whereas the highest molybdenum contents are from the lower part of the 

northern fork. 

Pan concentrates collected from this area by 

the U.S. Geological Survey in 1951 and 1952 

(Gault and others, 1953) in a search for uranium, showed anomalously high concentrations 

of uranothorianite as well as a variety of other 

metallic minerals such as galena, cralcopyrite, 

bornite, tetradymite, sphalerite, pyrite (up to 

50 percent of the concentrate), and pyrrhotite. 

Intergrowths of galena, sphalerite, chalcopyrite, pyrite, and gummite (probably a decomposition product of uranothorianite) were observed in some mineral grains (Gault and 

others, 1953, p. 29). The source c f the uranothorianite and associated sulfide;;- was not 

found during the 1951-52 investi~~ations, although West (in Gault and others, 1953, p. 

29-30) suggested a lode deposit at the head of 

the Peace River. The present study shows that 

the syenite and associated quartz veins exposed 

near the junction of the two main forks both 

contain anomalous amounts of molybdenum, 

bismuth, silver, copper, and lead. These deposits, and probably similar ones upstream, are 

the most likely source of the sulfide:~ and uranothorianite found in the pan concentrates. 

The association of uranium, silv~r, molybdenum, "bismuth, copper, and lead s~en here is 

typical of many uranium-bearing veins elsewhere in the United States ("~~alker and 

Adams, 1963). 

65" 

27' 

30" 

APPROXIMATE MEAN 

DECLINATION, 1969 

161"00' 

1 MILE 

FIGURE B.-Location of stream-sediment srmples of the 

upper Peace River area. 

13 
The relationship, if any, between the deposits 

of lead, zinc, and silver at Quartz Creek and 

the deposits in the upper Peace River drainage 

is unknown. The absence of tourmaline and 

arsenopyrite (and therefore low boron and 

arsenic content), the low tin content, and the 

presence of abundant fluorite in the upper 

Peace River deposits suggests that the two 

deposits are not genetically related. 

Because of the very poor exposures and short 

time spent in this investigation, it is not possible to give a complete evaluation of the potential of this area. However, a considerable area 

of high concentrations of a wide variety of 

metals has been outlined and is thought to be 

worthy of further exploration. A trenching 

and stripping program near the junction of the 

two main forks of the Peace River and also in 

their headwaters would help define the extent 

and amount of mineralized rock. Drilling may 

be necessary in areas with a thick overburden. 

BEAR CREEK 

Galena, sphalerite, and pyrite have been reported in andesite at the north end of the airstrip on Bear Creek north of the Granite Mountain pluton (fig. 1). The sulfides occur in 

quartz-calcite veinlets and as disseminated 

grains in the andesite near a mafic syenite dike 

(Herreid, 1965). The mineralized zone is about 

200 feet wide and tren<Js northwest. Gold can 

be panned from the limonitic capping over the 

mineralized rock. Stream-sediment samples 

downstream from the mineralized zone show a 

lead-zinc-copper anomaly extending for about 

a mile. Soil samples from a drainage ditch 

above the deposit contain anomalous lead and 

zinc and are thought by Herreid to indicate 

additional mineralization in the area. Placer 

gold has been mined on Bear Creek, particularly 

downstream from the mineralized area, off and 

on for over 60 years. 

The deposit was reexamined during the present investigation. Little can be added to Herreid's account except that polished-section 

study shows that arsenopyrite, bournonite, and 

a little gold are also present in the sulfide aggregate. Analyses of mineralized rock samples 

are given in table 4 and show anomalous lead, 

14 

zinc, silver, arsenic, cadmium, gold, copper, 

and antimony. 

The mafic syenite dike described by Herreid 

appears to be a biotite pyroxenite containing 

potassium feldspar and is similar to pyroxenite 

occurring along the edge of the Granite Mountain pluton. 

The Bear Creek deposit is not well enough 

exposed to evaluate its potential at t.he present 

time. However, the deposit is of inter~~st because 

of the mineralogical and chemical differences 

between it and the Quartz Creek deposit. The 

lead-zinc· deposit at Bear Creek occurs entirely 

in andesite and has anomalously higr antimony 

(samples 2-6, table 4) and gold, whereas boron 

and tin are quite low in direct contr·ast to the 

high boron and anomalous tin in the Quartz 

Creek lead-zinc deposit. Thus, a different origin 

for the two deposits is suggested. 

SUMMARY 

Investigation of the Granite Mountain area 

located two new mineralized areas thought to 

be worth further exploration. Both areas are 

related, at least spatially, to felsic plutonic 

rocks. The deposits in the Quartz Creek area 

are scattered over an 18-mile-long zone roughly 

parallel to prominent lineaments iiJ the area 

and centered around an altered quartz monzonite. The deposits in the upper Peace River 

drainage are disseminated in a syenitic stock 

satellitic to the Granite Mountain :t: 1uton and 

cut by mineralized quartz veins. f!tudies of 

stream-sediment samples in this area indicate 

anomalous metal contents over an area of about 

2 square miles. More detailed surface: prospecting together with geochemical and g1~ophysical 

surveys, trenching, and drilling will be necessary to determine the extent and ~,mount of 

mineralized rock. 

REFERENCES CITED 

Gault, H. R., Killeen, P. L., West, W. S., and others, 

1953, Reconnaissance for radioactive deposits in 

the northeastern part of the Seward Peninsula, 

Alaska, 1945-47 and 1951: U.S. Geol. Survey Circ. 

250, 31 p. 

Harrington, G. L., 1919, Mineral resources of Alaska, 

report on progress of investigations in 1917: U.S. 

Geol. Survey Bull. 692, p. 353-408. 
Herreid, Gordon, 1965, Geology of the Bear Creek area, 

Seward Peninsula, Candle quadrangle, Alaska: 

Alaska Div. Mines and Minerals Rept. 12, 16 p. 

Miller, T. P., Patton, W. W., Jr., and Lanphere, M. A., 

1966, Preliminary report on a plutonic belt in 

west-central Alaska, in Geological Survey research 

1966: U.S. Geol. Survey Prof. Paper 550-D, p. 

D158-D162. 

Moffit, F. H., 1905, The Fairhaven gold placers, Seward 

Peninsula, Alaska: U.S. Geol. Survey Bull. 247, 

85 p. 

Patton, W. W., Jr., 1967, Regional geologic map of the 

Candle quadrangle, Alaska: U.S. Geol. Survey 

Misc. Geol. Inv. Map I-492, scale 1:250,000. 

Patton, W. W., Jr., and Miller, T. P., 1968, Regional 

geologic map of the Selawik and southeastern 

Baird Mountain quadrangles, Alaska: U.S. Geol. 

Survey Misc. Geol. lnv. Map 1-530, scale 1 :250,000. 

15 

Patton, W. W., Jr., Miller, T. P., and Tailleur, I. L., 

1968, Regional geologic map of the Shur-rnak and 

southern part of the Ambler River quadrangles, 

Alaska: U.S. Geol. Survey Misc. Geol. lnv. Map 

1-554, scale 1:250,000. 

Sainsbury, C. L., 1964, Geology of the Lost F~ver mine 

area, Alaska: U.S. Geol. Survey Bull. 1129, 80 p. 

Sainsbury, C. L., and Hamilton, J. C., 1967, Geology of 

lode tin deposits: lnternat. Tin Council, 35 p. 

Smith, P. S., and Eakin, H. M., 1911, A geologic reconnaissance in southeastern Seward Peninsula 

and the Norton Bay-Nulato region, Alaska: U.S. 

Geol. Survey Bull. 449, 146 p. 

Walker, G. W., and Adams, J. W., 1963, Mineralogy, 

internal structure and textural characteristics, and 

paragenesis of uranium-bearing veins in the conterminous United States: U.S. Geol. Survey Prof. 

Paper 455-D, p. 55-90. 
TABLE 1.-Analyses of bedrock and 

[Results reported in parts per million. Gold by atomic-absorption analysis; all other elements are by semiquantitative spectrographic analysis with results 

than value shown; L, presert. but below limit of 

Sample Field 

locality No. Ag As Au B Ba Bi Cd Co Cr Cu 

l_ ______ 68AMm236A L L N G(2, 000) 300 N N 20 15 200 2A ______ 235A .5 500 N 2,000 500 N N 30 20 70 2B ______ 235B L *G(lO,OOO) .06 G (2, 000) 150 20 N 300 15 100 

3A ______ 68AEr124A 1.5 N N *G (2 ,000) 70 N 100 10 15 300 3B ______ 124B 20 N N *G (2,000) 150 N 150 20 15 300 4 _______ 68AGk82 N 3,000 N G(2,000) 500 L N 20 20 70 5 _______ 80 N N .2 G (2,000) 3,000 N N 15 L 70 6 _______ 68AMm372 .5 L N 150 200 N N 150 70 150 7 _______ 373A L L N *G (2,000) L N N 20 70 150 8 _______ 68AGk44A .7 300 N *G(2 ,000) 100 N N 5 70 70 9 _______ 43 L L N G(2,000) 50 N N 150 20 700 lOA _____ 41 N 500 N *G(2,000) 70 N N 15 700 200 lOB _____ 40 L 1,500 N *G(2 ,000) 100 N N 100 500 150 lL _____ 38 7 *G (10,000) .1 *G (2,000) L N N 500 70 300 12 ______ 37 7 *G(lO,OOO) N *G(2,000) L N N 10 300 150 

13 ______ 36 N 10,000 N *G(2,000) L N N 100 150 15 

14A _____ 68AMm240 N N N 1,000 1,500 N N 10 70 500 14B _____ 360A N L N 30 700 N N 15 70 150 14C _____ 360B N N N 50 1,500 L N L 20 150 15 ______ 68AEr126 N N N 300 1,500 N N 10 100 150 16 ______ 125 L N N 300 1,500 N N 10 70 100 17 ______ 68AGk34 1.5 G(lO,OOO) N *G(2, 000) 150 N N 10 15 70 

18A _____ 68AMm212A 1 N N 15 150 N N N 70 20 18B _____ 212B N 5,000 N 1,500 1,500 N N 15 15 100 18C _____ 68AErl16 50 N N 300 300 N G(500) 50 70 2,000 19A _____ 68AGk31A 200 700 .06 G (2, 000) 300 N 150 50 7 500 

19B _____ 31B 150 3,000 .2 *G(2 ,000) 70 N 300 100 10 1,000 20A _____ 29 7 N N *G(2,000) 150 N 50 L 15 300 20B _____ 68AMm213B 30 N N *G(2,000) L N 100 L 70 500 20C _____ 213C 7 N N *G(20,000) L N N N 15 70 21A _____ 210A 100 5,000 N 30 L 70 N L 70 700 21B _____ 210C 150 L N 30 70 L N 10 70 700 22 ______ 370 20 N N 10 300 L N 15 150 200 23 ______ 68AGk52 2 N N 30 L N L 10 70 500 

24 ______ 50 50 N N 700 150 N 150 50 300 700 25A _____ 68AMm470 20 N N 70 20 N 100 5 30 200 25B _____ 470 1 44 25C _____ 68AGk151A 3 300 N 300 300 N 50 30 150 100 26 ______ 51 150 N N *G(2,000) L N 100 10 200 1,500 

27_----- 68AMm215B 200 N N *G(2,000) 50 300 G(500) 100 150 200 28A _____ 68AErl27A L L N 2,000 L L N 70 300 150 

28B _____ 127B 1 *G(10,000) .2 *G(2,000) 300 300 N 2,000 15 500 29 ______ 68AGk144 7 N N G (2, 000) 300 10 N 7 150 150 30 ______ 143 1 N N 50 500 L N 20 200 150 31A _____ 68AMm214A 3 N N 70 50 N N 10 50 70 31B _____ 214C 300 5,000 N *G (2 ,000) L N G(500) 20 70 200 32 ______ 68AGk47 L N N 500 1,000 N N 10 100 70 33A _____ 45 N N N 500 700 N N 50 700 100 33B _____ 68AHd227 L L N 200 300 N N 20 150 150 34 ______ 226 150 L N 1,000 100 N *G(500) 150 150 500 35 ______ 68AMm221A 3 N N 70. 5,000 N 500 5 7 500 36 ___ . ___ 228 L L N 2,000 700 N N 15 150 500 37 ______ 227 L 3,000 1 *G (2,000) 150 20 N 30 300 300 38 ______ 68AHd56 N N N G(2,000) 150 N N 150 700 500 39 ______ 61 N N N *G(2,000) L N N 50 70 700 40 ______ 63 7 N N 500 300 N N 150 700 500 41_ _____ 244 N G (10, 000) .2 2,000 700 N N 150 500 300 42 ______ 65 .5 *G(10,000) .7 G(2,000) 200 20 N 150 70 300 

43 _ __-_--- 67 7 200 N 700 300 N N 150 700 500 44 ______ 73 L 1,000 N 700 300 N N 70 700 200 45A _____ 74 L 1,500 .04 1,500 300 N N 70 700 300 

45B _____ 75 5 500 N 70 300 N N 15 3,000 70 46 ______ 68AMm469 7 700 N *G(2,000) 70 N N 50 200 1,000 47 ______ 368 3 1,500 N *G(2,000) 100 L N 20 15 300 

Limits of determination __ 0.5 200 0.02 10 50 10 50 10 10 10 

Bedrock values considered 

anomalous in this report ________________ 0.5 L 0.04 50 2,000 10 L 150 300 209 

1 Analysts: Claude Huffman, J. A. Thomas, and V. E. Shaw; silver and zinc by atomic absorption, lead by electrolytic methods. 

16 
soil samples from Quartz Creek area 

reported to the nearest number in the series 1, 0.7, 0.5, 0.3, 0.2, 0.15, 0.1. N, not detected; H, interference; *G, much greater than value sho"ll·n; G, greater 

determination. Sample localities shown in fig. 2] 

Mo Mn Nb Ni Ph Sb Sn Sc w Zn Type of sample 

5 3,000 15 30 200 N N 100 N 1,000 Composite grab. 

N 2,000 L 50 700 L N L N L Do. 

L 5,000 L 70 150 L N 100 N N Grab; float. 

N G (5,000) L 10 1,500 N N 15 N G(10, 000) Grab. 

N 2,000 L 30 G (20, 000) L L 20 N G(10,000) Grab. 

N 2,000 10 15 150 N N 20 N 1,500 Select,'ld grab. 

N 700 L 7 50 N N 5 N N II'). 

L 2,000 L 50 300 L N 15 N 1,500 Comp')site grab. 

N 700 L 50 300 150 L 20 N 500 Grab. 

N G(5, 000) L 15 150 500 N 15 N N Comp')site grab. 

5 300 10 50 70 N L 70 N N [,'). 

N 700 L 150 10 N H(70) G (100) N L I' I. 

N 3,000 L 150 300 N N G(100) N N I' I. 

5 150 L 100 10,000 100 L 100 N 200 Grab. 

5 3,000 L 70 7,000 H (300) N 100 N 700 Grab. 

5 150 L 50 100 L 30 70 N L Selected grab; 

float. 

N 3,000 L 30 50 100 N 50 L L Composite grab. L 150 L 30 20 L N 20 N L Do. 

N 150 L 70 10 N N 20 N N Grab. 

N 500 L 30 150 N N 50 N L Soil. 

N 300 L 10 15 N N 50 N N Soil. 

N 150 10 5 1,500 L N L L 300 Selected grab; 

float. 

5 G(5,000) L L 700 N N N N L Comrosite grab. L 200 L 5 150 N N L N 300 Do. 

N G (5,000) L 10 *G(20,000) N H(20) L N *G(10,000) Grab. 

L G(5,000) 10 50 *G (20, 000) 100 H(30) L N *G (10, 000) Grab. 

L 300 L 30 *G(20,000) 150 H(30) L N *G (10, 000) Grab. 

20 5,000 10 5 7,000 L H(30) 5 N 3,000 Grab; float. 

30 2,000 L 20 G(20,000) N 20 5 N 5,000 Comrosite grab. N 5,000 L L 15,000 L N N N 1,000 Do. 

L 150 L 10 *G(20, 000) 100 30 5 N 7,000 Do. 

15 500 L 70 G(20,000) 150 20 10 N G(10, 000) Do. 

L 3,000 L 30 15,000 100 N 10 N 700 Selected grab. 

N G(5, 000) L 30 7,000 N N 10 N 10,000 Selected grab; 

flor.t. 

N 5,000 L 70 1,500 N H(10) 20 N *G (10, 000) Do. 

N G(5, 000) N 30 15,000 200 150 30 N G (10, 000) Composite grab. 1 22,500 1 46,700 Do. 

N 5,000 N 50 500 L 30 20 N G (10, 000) Chip sample. 

N G (5, 000) L 70 20,000 N H(50) 15 N G(10,000) Selected grab; 

flor.t. 

N 3,000 L 70 *G(20,000) 150 N 30 N *G(10,000) Composite grab. 

7 G(5,000) 10 100 150 N 50 15 N 3,000 Composite grab. 

7 3,000 L 150 200 700 30 30 L L Grab. 

5 300 L 30 1,000 L 70 20 N 1,000 Composite grab. 

N 1,000 L 100 1,500 N N 30 N 1,500 Soil. 

N G(5,000) L 50 5,000 L H(15) 10 N 300 Composite grab. 

N 5,000 L 50 *G(20,000) 500 H(70) 30 N *G(10,000) Grab. 

N 200 L 50 300 N 10 20 N L Soil. 

N 700 L 100 150 N 10 50 N L Soil. 

N 3,000 L 100 300 L L 30 N 300 Composite grab. 

N 5,000 L 150 G(20,000) 150 500 15 N *G(10,000) Do. 

7 5,000 L 20 *G(20,000) N N 15 N G(10,000) Grab. 

7 1,500 15 70 150 N N 50 G(10,000) N Composite grab. 

N 300 10 100 150 N 300 50 L N Do. 

N 1,500 L 300 150 N N G(100) N L Soil. 

5 300 L 50 150 N N G(100) N L Composite grab. 

N G (5, 000) 10 300 7,000 N N G(100) N 10,000 Soil. 

N 3,000 L 150 150 N N 100 N L Soil. 

7 2,000 L 70 700 300 N 20 N 200 Composite grab. N G(5,000) L 300 300 N N 100 N 500 Soil. 

N 2,000 L 200 700 N N 100 N 1,500 Soil. 

N 1,500 L 200 150 N N 100 N L Soil. 

N G(5,000) L 200 7,000 N N 100 N 10,000 Comoosite grab. 

15 300 L 70 300 100 70 30 N 700 Grab. 

N 700 L 70 200 L 30 15 100 500 Grab. 

7 10 10 5 10 100 10 5 50 200 

10 3,000 50 200 150 L 30 50 L L 

17 
TABLE 1.-Analyses of bedrock and soil samples from Quartz Creek area-Continued 

Sample 

l ____ ------- 2A _________ _ 2B _________ _ 

3A _________ _ 3B _________ _ 

4, 5 ________ _ 6 __________ _ 

7 __________ _ 8 __________ _ 

9, lOA _____ _ 

lOB ________ _ 

11, 12 ______ _ 13 _________ _ 

14A, B, C __ _ 17 _________ _ l8A _____ ----

18B ________ _ 18C ________ _ 

19A _______ _ 19B ________ _ 

20A ________ _ 

2oB, c _____ _ 

Description 

Gossan in altered andesite. 

Pyrite-calcite vein 6 inches wide. 

Float; arsenopyrite and quartz. 

Talus; quartz vein with sphalerite. 

Talus; quartz vein with galena and sphalerite. Altered andesite. 

Pyrite-bearing calcite vein. 

Calcite veinlet cutting andesite; minor galena. 

Pyrite-tourmaline-carbonate rock in 100-yard-long altered zone. Pyrite-tourmaline veinlets 1 inch thick in altered ande- site. Talus over 300 yards along creek; sulfide-bearing tourmaline-rich rock. 

Sulfide-bearing tourmaline-quartz rock. 

Float; silicified breccia with arsenopyrite. 

Silicified, extensively oxidized rhyolite. 

Float; sulfide-bearing tourmaline-quartz rock. 

Pyrite-calcite vein 1 foot thick cutting altered fine- grained felsic intrusive. 

Fine-grained felsic intrusive; altered. 

Talus; sphalerite-galena-calcite vein; angular blocks up to 1 foot long. 

Talus; galena-bearing gossan. Talus; quartz-pyrite-arsenopyrite vein. 

Float; sulfide-bearing quartz. 

Float; sulfide-bearing gossan. 

Sample 

21A, B _____ _ 

22_- -------- 23, 24 ______ _ 

25A ________ _ 25B ________ _ 26 _________ _ 

27---------- 28A, B _____ _ 28B ________ _ 

29------- ---

31A ________ _ 31B ________ _ 

33B ________ _ 34 _________ _ 35 _________ _ 

36_---------

37----------

39_---------

42_--------- 45B ________ _ 

46_---------

47----------

Description 

Gossan with visible galena; several gossans up to 4 feet wide in quartz monzonite. 

Galena-bearing calcite vein 1 foot thick. 

Float; large boulders up to 1 foot in diameter; quartz- carbonate-sulfide rock. 

Galena-bearing calcite vein 18 inches thick. 

Sulfide-carbonate-quartz rock. 

Float; quartz-carbonate-sulfide rock. 

Sulfide-bearing oxidized carbonate in altered andesite. 

Float, talus(?); pyrite-bearing quartz. 

Talus; altered andesite containing arF<:>nopyrite, realgar, and orpiment. 

Sample from over 200- by 200-foot area of gossan and altered andesite. 

Oxidized carbonate-rich gossan in altered andesite. 

Galena-bearing gossan. - Oxidized rubble in frost boil. 

Galena-sphalerite-pyrite-quartz veins in altered andesite. 

Talus; disseminated galena in oxidize« carbonate-quartz 

rock. 

Talus; disseminated pyrite and scheelite in quartz. Gossan along quartz monzonite-andes'te contact. Oxidized quartz-tourmaline rubble. 

Oxidized rubble in frost boil. 

Talus(?); disseminated galena in oxidized quartz- carbonate rock. 

Oxidized pyrite-tourmaline vein. 

Oxidized breccia. 

TABLE 2.-Analyses of bedrock and soil samples /'rom the Upper Peace Ri·ver area 

[Results reported in parts per million. Gold by atomic-absorption analysis; all other elements by semiquantitative spectrographic an11lysis with results reported to the nearest number in the series 1.0, 0.7, 0.5, 0.3, 0.2, 0.15, O.l. N, not detected; *G, much greater than value shown; G, greater than value shown; L, present but below level of determination. Sample localities are shown in fig. 7] 

Sample Field locality No. Ag Au B Bi Cu Mo Pb Sn w Zn Remarks 

l __________ 68AHd99 N 0.04 30 N 200 N 30 N N N Altered andesite; con'1>osite grab 

2 __________ 103 5 N 15 *G (1 ,000) 300 150 300 L N N samEle. 

Pyriti erous oxidized syenite; com3 _________ - posite grab sample" 104 150 .04 20 *G (1 ,000) 700 30 3,000 N N N Do. 4 __________ 189 1 N 10 300 200 150 150 10 N N Oxidized syenite witl pyritiferous 

quartz veinlets; corrposite grab 

5 __________ samtle. 68AMm361G N 10 *G(l,OOO) 300 1,500 150 L N L Pyriti erous quartz in oxidized syenite; 

6 __________ 68AHd105 composite grab sazrnle. 1.5 N 30 300 500 G(2,000) 300 N N N Oxidized syenite(?); composite grab 

7 __________ samtle. 186 N 15 10 200 1,000 150 15 N N Pyriti erous quartz v'~ins in oxidized 

8---------~ 185 1.5 N 10 70 200 200 150 20 N N syenite; com:posite grab sample. 

Pyritiferous o:ndized syenite; com9 __________ 184 .7 N 30 L N posite grab sample. 10 100 30 70 10 Do. 10 _________ 68AMm361C L N 20 150 150 15 20 L N N Do. 11--------- 361A 1.5 N L 15 300 200 20 N N N Do. ll _________ 361B 7 N L 20 200 100 20 30 N N Do. 12--------- 473 L N 30 15 300 30 100 10 N N Oxidized fine-grained syenite; com13 ____ ----- 68AGk160 posite grab sample. 3 N 100 20 20 70 150 L N N Oxidized syenite; sele~ted grab sample. 14 _________ 68AMm362 L N 20 30 150 30 150 15 L N Pyritiferous quartz in syenite; com15 ____ ----- 68AGk155 N 200 posite grab sample. 7 20 150 15 300 L 30 L Oxidized :ftuorite-bearng pyritiferous 

16 _________ 63 N N 70 syenite; selected grab sample. N 50 N 100 N N L Soil samples. 17 _________ 154 N N 70 L 30 15 70 N N N Do. 18 _________ 155 1 N N 15 500 70 300 N N N Do. 19 ______ --- 156 N N 30 N 200 50 200 N 70 N Do. 20 _________ 158 N N 70 N 150 30 150 N N N Do. 21 _________ 159 N N 30 15 200 30 150 N N N Do. 22 _________ 160 15 N 200 70 200 30 1,000 N N N Do. 

Limits of determination _____ 0.5 0.02 10 10 5 5 10 10 50 200 

Bedrock values considered anomalous in this report__ 0.5 0.04 50 10 200 10 150 30 L L 

18 
(i) 

, 

0 

00 

-.1 

0 

U1 

N 

• 

1--L 

~ 

TABLE 3.-Partial analyses of stream sediment samples from the upper Peace River area 

[Results are reported in parts per million. Analyses are by semiquantitative spectrographic methods with results reported to the nearest number in the 

series 1.0, 0.7, 0.5, 0.3, 0.2, 0.15, 0.1. N, not detected; L, present but below limit of determination. Sample localities shown in fig. 8] 

Sample locality Field No. Mo Cu Pb Ag Sample locality Field No. Mo Cu Pb Ag 

1 _____________ 68AHd197 N 50 30 N 16 ____________ 68AHd213 N 300 10 N 2 _____________ 68AEr193 N 15 150 N 17 ____________ 88 N 15 15 N 3 _____________ 243 7 30 100 N 18 ____________ 94 N 100 15 N 4 _____________ 68AGk66 7 70 100 L 19 ____________ 95 15 100 100 N 5 _____________ 65 L 30 500 L 20-- _'_-------- 214 N 30 30 N 6 _____________ 157 30 150 200 N 21_ __ --------- 98 N 150 15 N 7 _____________ 67 10 70 300 .7 22 ____________ 100 7 100 30 N 8 _____________ 69 15 30 300 .7 23 ____________ 196 N 30 70 N 9 _____________ 68 15 30 150 L 24 ____________ 195 N 70 20 N 10 ____________ 70 30 300 150 .5 25 ____________ 194 N 100 70 N 11 ____________ 71 30 150 150 L 26 ____________ 190 N 150 70 N 12 ____________ 68AHd204 N 15 100 N 27 ____________ 106 N 70 70 N 13 ____________ 205 N 100 L N 28 ____________ 68AEr246 L 10 30 N 14 ____________ 210 N 200 20 N 29 ____________ 200 7 200 150 N 15 ____________ 211 N 150 L N 30 ____________ 201 N 100 100 N 

Limits of determination _____ 5 5 10 0.5 Limits of determination _____ 5 5 10 0.5 

TABLE 4.-Analyses of bedrock samples from the Bear Creek prospect 

[Results reported in parts per million. Gold by atomic-absorption analysis; all other elements by semiquantitative spectrographic analysis with results reported to the nearest number in the series 

1.0, 0.7, 0.5, 0.3, 0.2, 0.15, 0.1. N, not detected; *G, much greater than value shown; G, greater than value shown; L, below limit of determination] 

Sample Field No. Ag As Au B Ba Bi Cd Co Cr Cu Mo Mn Nb Ni Pb Sb Sn Sc Zn 

1 _______ 68AGk95 1.5 *G(10,000) 3.0 30 500 L N 70 100 50 N 2,000 10 30 200 L N 30 1,000 2 _______ 98 50 2,000 .8 30 L 10 L 50 100 500 N G(5,000) 10 50 20,000 3,000 N 50 3,000 3 _______ 175D 30 500 1.4 20 20 10 N 15 30 200 N 2,000 N 30 20,000 1,000 N 7 700 4 _______ 175E 30 1,000 1.2 30 150 N 150 15 70 150 5 G(5,000) L 50 *G(20,000) 1,000 N 10 G(10,000) 5 _______ 175F 150 1,500 1.1 20 20 10 200 20 50 1,000 N 2,000 N 50 G (20,000) 1,000 N 10 G(10,000) 6 _______ 175G 30 3,000 .4 30 700 N 70 15 70 500 7 G(5,000) 10 70 "G (20,000) G (10,000) N 15 G (10,000) 7 _______ 175H 150 7,000 .7 30 150 N 150 10 70 500 7 G (5,000) 10 30 *G (20,000) *G(10,000) N 7 G(10,000) 

Limits of determination:.._ 0.5 100 0.02 10 50 10 50 10 10 10 7 10 10 5 10 100 10 5 200 

Bedrock values considered 

anomalous in this report ________________ 0.5 L 0.04 50 2,000 10 L 150 300 200 10 3,000 50 200 150 L 30 50 L 

Sample Description Sample Description 

1 ___________ Selected grab sample oi oxidized andesite float; contains 10 to 15 percent sulfirle. 5 ___________ Gr<1.h 'l<l.mi>h~ from 12-inch-thick vein of galena, pyrite, and sphalerite in quartz- 2 ___________ Selected grab sample of andesite along 100-yard-long altered zone in creek bank. carbonate gangue. g ___________ Chip sample over 11 feet of andesite in cutbank. Visible pyrite, arsenopyrite, and 6 ___________ Composite grab sample from pyrite-galena-bournonite veinlets in altered andesite. 

galena in quartz-carbonate gangue. Collected over 10- by 30-foot area. 4 ___________ Chip sample over 18 feet of oxidized andesite. 7 ___________ Selected grab sample from 8-inch-thick pyrite-galena-quartz-carbonate vein in 

andesite.