BULLETIN 86

Geology and Ore Deposits of the
Sacramento (High Rolls) Mining
District, Otero County, New Mexico
By S. K JEROME, DOUGLAS D. CAMPBELL,J A C K S . WR I G H T , A N D H O WA R D E . V I T Z

1965

STATE BUREAU OF MINES AND MINERAL RESOURCES
NEW MEXICO INSTITUTE OF MINING & TECHNOLOGYCAMPUS STATIONSOCORRO, NEW MEXICONEW MEXICO INSTITUTE OF MINING & TECHNOLOGY
Stirling A. Colgate, President

STATE BUREAU OF MINES AND MINERAL RESOURCES
Alvin J. Thompson, Director

THE REGENTS
MEMBERS Ex OFFICIOThe Honorable Jack M. Campbell ...................... Governor of New Mexico
Leonard DeLayo .................................... Superintendent of Public Instruction
APPOINTED MEMBERS

William G. Abbott ........................................................................... Hobbs
Eugene L. Coulson, M.D. ............................................................. Socorro
Thomas M. Cramer ....................................................................... Carlsbad
Eva M. Larrazolo (Mrs. Paul F.) ......................................... AlbuquerqueRichard M. Zimmerly .................................................................... Socorro

For sale by the New Mexico Bureau of Mines and Mineral Resources
Campus Station, Socorro, N. Mex.—Price $2.00

Contents
Page
ABSTRACT ..................................................................................................... 1
INTRODUCTION ........................................................................................ 2
Geography .................................................................................................... 2
Methods of investigation ........................................................................... 3
Acknowledgments ....................................................................................... 4
GEOLOGIC SETTING ............................................................................... 6
Regional geology ......................................................................................... 6
Stratigraphy and structure ..................................................................... 6
Intrusives ................................................................................................. 7
The Abo Formation .................................................................................... 7
Distribution ............................................................................................. 7
Stratigraphy .............................................................................................. 8
Structure ................................................................................................... 9
MINERAL DEPOSITS .............................................................................. 11
Production ................................................................................................. 11
Mineralization ........................................................................................... 11
Lead ....................................................................................................... 11
Copper ................................................................................................... 12
Other minerals ..................................................................................... 13
Mines and prospects ................................................................................ 14
Warnock area ........................................................................................ 14
Geology .............................................................................................. 15
Sampling results ................................................................................ 17
Warnock mine ................................................................................... 17
East Warnock workings ................................................................... 19

Page
Red Hill .................................................................................................... 19
Sacramento Gulch area .......................................................................... 20
Lower Karr Canyon ............................................................................... 22
Sacramento Gulch to Courtney mine .................................................. 22
Courtney mine ......................................................................................... 23
Courtney mine to Arcente Canyon ...................................................... 23
Speckled Bird Nose ................................................................................ 24
Warnock Extension to Ady mine ........................................................ 24
Ady mine area ......................................................................................... 25
Ore genesis ................................................................................................. 26
Discussion and conclusions .................................................................. 27
REFERENCES .............................................................................................. 30

Illustrations
PLATES(All plates are in the pocket)

1.

Location of the Sacramento (High Rolls) mining district2.

Index map to plates

3.

Reconnaissance map of the Abo Formation

4.

Surface geology, Warnock area

5.

Results of KI testing, Warnock surface area

6.

Results of sampling and KI testing, East Warnock bulldozer cut

7.

Plan and sections of the Warnock mine

8.

Assay map, Warnock mine

9.

Block diagram of the Warnock mine

10. Geology and assay map, East Warnock area
11. Assay map, Red Hill area

12. Surface geology, Sacramento Gulch area
13. Geology and assay map, Sacramento Gulch area
14. Assay map, Courtney area
15. Assay map, Black Bear prospect
16. Geology and assay map, Arcente Canyon area
17. Geology and assay map, Warnock Extension area
18. Geology and assay map, Ady area

Abstract
In the Sacramento (High Rolls) mining district, Otero County, New
Mexico, the Permian Abo Formation unconformably overlies foldedand faulted rocks of pre-Permian age; in turn, it is overlain conformably(?) by the Permian Yeso Formation. Structure in the Abo and Yeso
is relatively simple, being generally a monocline striking north anddipping gently east and cut by faults of moderate throw. The few intrusives in the district are sills of andesite with no associatedmineralization or alteration.
The Abo contains small, irregular deposits of copper and lead minerals occurring separately or associated in discontinuous, light-coloredarkose beds sandwiched between red shales. Total production from these
deposits through 1962 probably does not exceed 23,000 tons of lead ore
varying between 5 and 11 per cent lead and 6500 tons of copper ore
varying between 2 and 7 per cent copper. Minor amounts of other metals
occur with these principal ore types.
Evidence accumulated as a result of surface and underground mapping, a large number of assays, and extensive testing of favorable-appearing arkose beds with acetic acid and potassium iodide for lead sulfate andlead carbonate strongly suggests that the ores are "semisyngenetic" inorigin. Copper and lead sulfides possibly were deposited with the arkose.
The source of the metals has not been established. Both copper and leadsulfides later were oxidized and the metals reconcentrated to some extent
as carbonates and sulfates by the action of ground water.
Provided such an origin is correct, the overlying Yeso Formation andthe underlying rock units, predominantly the Magdalena Group, containno ore deposits that are genetically related to those in the Abo.

Introduction
In 1948, the New Jersey Zinc Company became interested in scattered lead and copper occurrences in the Abo Formation on the western
flank of the Sacramento Mountains, New Mexico (pl. 1). Investigations
were designed in 1948 and 1949 to evaluate the known lead and copperore bodies, to seek additional deposits, and to establish, if possible,
whether the ores are hydrothermal in origin. If such could be demonstrated, it was planned to seek replacement ore bodies in limestone
beds overlying and underlying the Abo.
Work on this manuscript was initiated some years ago at the requestof Eugene Callaghan, former director of the New Mexico Bureau of
Mines. It was undertaken with the permission and encouragement ofWilliam H. Callahan, manager of exploration for the New Jersey Zinc
Company, but because of the press of other assignments, the task was
not completed. Its reactivation is due to the following observation madein 1963 by Mr. Callahan to the senior writer: "Now that the genesis ofstratiform ore deposits is receiving increasing attention, and syngeneticists and epigeneticists are belaboring each other all over the world, perhaps it is timely to contribute additional concepts to the controversy."
Accordingly, this report, an abridgment of one submitted to the Company, describes the geologic setting of the stratiform ore deposits of the
Sacramento (High Rolls) mining district and reviews evidence pertinent
to their origin.
GEOGRAPHY
The Sacramento (High Rolls) district is on the western slope of the
Sacramento Mountains, east of Alamogordo, in the north-central part of
Otero County, New Mexico. The district is considered to extend fromRed Hill, half a mile north of High Rolls, to Alamo Canyon, seven miles
due south of High Rolls. A well-maintained forest road, locally known as
the West Side Road, branches from State Highway 83 near High Rolls
and provides access to much of the region.
Vegetation includes ponderosa pine, pinion, juniper, scrub cedar, andscrub oak of several types liberally interspersed on the lower sunny
slopes with a wide variety of spiny desert plants. Excellent fruit is grownin the vicinity of High Rolls.
Elevations in the district range between 6500 feet and 7500 feet,while those of the Sacramento Mountains as a whole range from 4200
feet at the western mountain front in the Tularosa Basin to 9500 feet atthe crest. This relief of 5300 feet makes for considerable variety in the
climate. Summers are hot and are characterized by sudden showers; coldand snow or rain can extend over several months during the winterseason.

SACRAMENTO (HIGH ROLLS) MINING DISTRICT3

METHODS OF INVESTIGATION
To provide a regional geological background for detailed work, ageneral reconnaissance was made from Alamo Canyon north to High
Rolls, using as mapping bases aerial photographs, a U.S. Forest Service
topographic map, and a property map prepared by Company personnel.
Results of this reconnaissance are presented on Plate 3. Some of thenames on this plate are from abandoned claim locations; they are included to facilitate discussion.
The beginning point of a transit survey designed to provide generalengineering control and to locate property was a U.S. Forest Service
bench mark labeled W-100 in the Warnock mine area. Co-ordinates
12,000 North and 10,000 East were assigned to W-100 so that all survey
calculations would fall in the northeast quadrant. Co-ordinates of allmaps included herein are related to this station (pl. 2). Four sets of solar
observations were made from this point, averaged, and referenced to
distant permanent objects. Traverses were run north and south from the
beginning point with side traverses made as needed. Bearings werechecked occasionally by solar observations. Ties were made to convenient section corners, using co-ordinates calculated from U.S. Bureauof Land Management plats that show bearings and distances; otherwise,
the traverses north and south were not closed. The U.S. Coast and Geodetic Survey adjusted elevation for W-100, based on second order leveling, is 7304.703 feet.
While engineering work was in progress, all workings in the district
known to contain either lead or copper minerals were cleaned out for
mapping and sampling. Additional exposures were made by open cuts,
trenches, shallow shafts, limited drifting, jackhammer holes, and bulldozer cuts.
The two principal areas of mineralization, Warnock and Sacramento Gulch, were mapped by alidade and plane table and studied inparticular detail. All open cuts, adits, and likely appearing exposures inthese and other areas were mapped and sampled. Attention was concentrated on the Dollins tunnel, Warnock mine, and Ady incline. (Theterm tunnel follows district practice, although the use is not technicallycorrect.)
Fairly coarse sampling techniques were used. Because of the ore type
involved, it was not believed necessary to cut precision channels, although at the Warnock mine an attempt was made to do this aided by anair sampling hammer. To ensure reasonable accuracy in assaying results,
a limited number of samples was run by two different chemists inseparate organizations; comparisons were quite satisfactory.
It was contended by those with mining experience in the district that
it is impossible to sample the arkose with any degree of accuracy. To test
the validity of this contention, the Warnock and Dollins work-

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NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

ings were chosen. Besides attempting to overwhelm the problem with alarge number of samples, range of vision was extended by the acetic
acid-potassium iodide test (KI) for oxidized lead minerals (Jerome,1950).
In making this test, a 5 per cent solution of acetic acid is applied bybrush, dropper, or spray to a relatively clean surface of the material inquestion and allowed to stand for 30 seconds to 1 minute. Then a 5 percent solution of potassium iodide is added. If anglesite or cerussite ispresent, the canary-yellow lead iodide precipitate appears. This method
was used on all sample sites, and locally, areas between samples were
tested on a wholesale basis. A critical analysis of the results indicatesthat samples taken give a satisfactory picture of the distribution andquality of the mineralization.
In the Warnock mine, the KI test, which is essentially qualitative,
was calibrated to known lead assays. A crude quantitative scale wasestablished whereby the intensity and speed of appearance of the yellow lead iodide precipitate could be noted quickly and a fairly clear
idea gained of the lead carbonate content. After such calibration, thetest was used extensively on outcrops, fly sprays and large pressure
garden sprays being used with equal satisfaction in applying the solutions.
Sulfidizing cerussite with a 10 per cent solution of Na 2 S was done
mostly as a curiosity during the latter stages of the investigation. In
another problem of this type, sodium sulfide would be useful in helping
to reveal the distribution of oxidized lead minerals and in calibrating KI
test results.
Nine samples representative of the mineralization in the district were
tested spectrographically in the New Jersey Zinc Company's laboratory at
Palmerton, Pennsylvania, and checked by Geiger counter for uranium
content.
ACKNOWLEDGMENTS
The writers express their appreciation to their former associates, A.
Merz, Jr., H. C. Summers, and Quentin Drunzer for their enthusiastic
and capable assistance in the field and office. M. F. Drunzer was mosthelpful in supplying information about the district and in conducting
certain exploration work for the Company. Beneficial field contacts were
had with other geologists, including Lloyd C. Pray, who mapped the
Sacramento Mountains, A. L. Bowsher of the Smithsonian Institution,
and Jerry Covington of the Humble Oil and Refining Company.
Critical review by William H. Callahan, W. P. Johnston, John H.
Schilling, Lloyd C. Pray, Frank E. Kottlowski, and George B. Griswold
has greatly improved the text and maps; such deficiencies as remain are

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

5

solely the responsibility of the writers. Most of the plates and figures
which originally illustrated the Company report have been redrafted andcolor separations made by Roland V. Wilson and Richard R. Paul.
Director Vernon E. Scheid of the Nevada Bureau of Mines generously allowed the senior writer time in 1964 to rework the original Company report for publication.
Finally, appreciation is expressed to officials of the New Jersey Zinc
Company and to all property owners (1949) who granted permission to
publish the information contained herein.

Geologic Setting
REGIONAL GEOLOGYSTRATIGRAPHY AND STRUCTURE

The rocks underlying the west front of the Sacramento Mountains in
the vicinity of Alamogordo represent a sedimentary section ranging inage from Cambrian(?) at the foot of the mountain front to Middle
Permian at the crest and on the eastern slopes. The following,
generalized from Darton (1928) and Pray (1961), is representative of thegross stratigraphic sequence near the mapped area:
ACE

PermianPermianPermianPennsylvanianMississippian
Devonian
SilurianOrdovician
Ordovician
Ordovician andCambrian 0
Precambrian

UNIT

THICKNESS (FEET)

San Andres Limestone
700
Yeso Formation
1200-1800
Abo Formation
100-700
Magdalena Group
2000-2500
Lake Valley Limestone
300-400
Onate, Sly Gap, and Percha formations 60-100
Fusselman Dolomite
100
Montoya Formation (including Valmont
Dolomite)
290-450
El Paso Limestone
430
Bliss Sandstone
Diabase, sandstone, and shale110--

In general, these formations are but gently tilted or folded, the exceptions being where regional stresses have produced local tight folding
and block faulting, particularly along the western mountain front. The
more prominent faults and fold axes have predominantly northward
trends. However, faults of moderate displacement striking northeast toeast have been noted. Dips in the Abo and Yeso generally are moderate
and to the east.
Pre-Permian deformation is expressed by folding and faulting of therocks underlying the lower Permian Abo Formation. The Abo lies
unconformably on the Pennsylvanian Magdalena Group, although insome places no angular discordance exists between them. In Arcente
Canyon, pre-Abo erosion removed the Pennsylvanian section, and theAbo rests directly on Mississippian limestone.
The Abo Formation crops out along the western range front just below the edge of the plateaulike top of the mountains. It ranges from anelevation of more than 8000 feet south of Alamo Canyon to less than
6500 feet at La Luz Canyon, twelve miles to the north. The formation islenticular, changing in thickness from less than 100 feet to nearly 700
feet. The thick Abo lenses represent pre-Permian structural andSACRAMENTO (HIGH ROLLS) MINING DISTRICT

7

topographic lows that were filled in Permian time. The thinner sections
represent highs that were veneered.
The contact between the Abo and the overlying Yeso often is exceedingly irregular, but no angular relationships can be observed
except in areas of what appear to be deep channel filling. Pray
(personal communication, 1949), who has examined a much larger area
than covered by this report, suggested to the writers that theirregularities at the base of the Yeso probably are not due to filling ofan erosion surface on the Abo but reflect the land sliding ofincompetent Yeso rocks across the contact. Although field evidence
for or against this belief is often ambiguous, the suggestion isincorporated on Plates 3, 4, and 12. The Yeso limestones, siltstones,
and gypsiferous beds are poorly exposed because of their tendency toweather rapidly and produce soils favoring the heavy growth of brushand trees. Often considerable breaking with little displacement isevidenced in the Yeso where exposed in road cuts. Occasionally suchzones lie along projected pre-Permian structures and suggest renewed
movement along these "basement" breaks, possibly in Laramide time.
Quite recent spring deposits consisting of travertine and calcareous
tufa occur in the Abo in Karr Canyon, on the Speckled Bird Nose, and in
the east Warnock area. These deposits are believed to correlate with early
regional ground-water activity which locally appears to have concentrated
commercial lead values and effected the redistribution of certain copper
minerals.
INTRUSIVES
The only intrusives found in the district are several hornblende
andesite sills that crop out in pre-Abo rocks between Alamo Peak andthe Warnock mine and between Alamo Peak and Alamogordo. Thesesills appear to be laccolithic, thickening from a few feet to a hundred feetin relatively short distances. Borders of the sills commonly show chilling,
but these intrusives produce no alteration of the enclosing rock except
for rare, narrow bands of bleaching.
Sills and dikes of similar composition are known in Magdalena
rocks in Ortega Peak east of the district, in the Abo in a road cut on
State Highway 83, and in the Magdalena Group north of High Rolls.
Neither significant alteration nor mineralization was observed near anyof these intrusives.
THE ABO FORMATION
DISTRIBUTION
From High Rolls to Alamo Canyon, the Abo Formation usually isrepresented by three distinct members; a coarse basal limestone or

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NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

quartzite conglomerate, a principal middle member comprising alternating arkose, siltstone, and shale, and an irregular capping of red
shales. The conglomerate and red shale members frequently are
missing or are obscured by slide rock. The distribution of thesemembers and the outline of the Abo from Alamo Canyon to High
Rolls are shown on Plate 3.
The Abo maintains a consistent thickness of about 200 feet along its
easternmost exposed edges, but in the Warnock—Speckled Bird area andthe Stark Nose—Alamo Canyon area, it extends westward and thickens
to about 700 feet, in both instances probably having filled local, prePermian basins. The eastern exposures are largely comprised of thearkose member and irregular thicknesses of the red shale member. The
basal conglomerate and the red shale attain their greatest thicknesses inthe two basins with a corresponding increase in thickness of the arkose
member. These variations in thickness do not appear to have affectedlead or copper distribution in the arkose, for the Warnock and Speckled
Bird deposits are in a basin while the Dollins, Tony, Courtney, and Ady
deposits all are in thinner sections of the Abo.
STRATIGRAPHY
Basal conglomerate member. The basal limestone conglomerate is locally
distributed in the basins, where it ranges from zero to several hundred
feet in thickness. It does not appear between the north Warnock area
and Red Hill, although Pray (personal communication, 1948) reports it
again north of Red Hill. In the southern area, it is composed of bedded
units of about 30 per cent sandy matrix and 70 per cent boulders andpebbles, about 80 per cent of which are limestone and 20 per centquartzite and quartz. The pebbles range in diameter from one quarterof an inch to four inches, their over-all average diameter being about
two inches. In some places, silty layers up to 2 feet thick occur in theconglomerate, but in the southern part of the district the member isfairly uniform. On Red Hill, north of High Rolls, it is predominantly
quartzose in character. This basal member usually is flat or dips veryslightly.
Arkose member. Though varying in thickness from 50 feet to 200 feet,this member is the most persistent of the three constituting the Abo.
Actually, only about 40 per cent of it is arkose; the bulk is composed of
red and chocolate shales and siltstones.
Arkose beds ranging from a few feet to 20 feet in thickness andaveraging about 6 feet are intercalated with the shales. The thicker
sections probably represent main parts of stream channels which crosscut
enclosing shales as diastems. One easily gains an erroneous impression as
to the amount of arkose in the underlying rock, for locally, where

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

9arkose beds are moderately concentrated, an entire area may be covered with arkose float blocks, the shale having been eliminated byerosion.
Differences in composition, grain size, and weathering produce several types of arkose. Where the mineral grains are almost entirely quartz,
the arkose is sugary and bleached in appearance. Quartz, feldspar, andcarbonate aggregates result in more compact and pink to yellow-brown
beds. Modest amounts of limonite occur in small brown spots or
blotches in these types, but where limonite is concentrated sufficiently,
it colors the arkose a chocolate brown. Occasionally, slightly
conglomeratic facies are found, but such coarse beds are minor and discontinuous. All types of arkose grade into shale, this being a generalcharacteristic over the entire region.
For detailed surface mapping, the arkose beds were divided into threecolor categories; cream, chocolate or purple, and red or light brown. A
careful study of specimens would be necessary to determine which of theseveral varieties is more likely to contain lead values, but observations so
far made permit a few general conclusions. Lead, in both sulfide andcarbonate forms, is most evident in light gray to pale yellow-brown,
medium-grained, compact arkose but also is found in similarly colored,
finer or coarser material. Since yellow limonite-spotted rock often carries
lead ore, such coloring and spotting at first appeared to be an ore guide.
However, much of the district is underlain by such favorable-appearing
arkoses that apparently are barren.
Red shale member. The red shale member at the top of the Abo varies
from zero to several hundred feet in thickness. This member is thinly
layered, brick-red, and varies in composition from shale to silt-stone.
Under the influence of gravity, these beds break up and creep
extensively so that the actual contact between them and the arkose
member beneath is somewhat difficult to fix. This also is true for the
YesoAbo contact.
STRUCTURE
Within the area described, the Abo displays considerable irregularity instrike and dip. These irregularities are due partly to sedimentation andpartly to deformation. To generalize, the most persistent strike trends areeither slightly west or east of north, except in basin areas, with east dips
predominating and ranging up to 25 degrees. In detail, gentle strike
terraces and synclines, best expressed in arkose beds, often warp the
monoclinal structure.
On the various plates, several faults are shown cutting the Abo. No
doubt many others have gone unmapped because of poor exposures, but
the displacements on them are not great enough to produce significant

10

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

discrepancies in the relations of the major units. No alteration or mineralization is visible on or near any of the faults observed, except for
the Warnock fault where an open cut reveals some bleaching of the red
shale.
Near-bedding plane movement is suggested by the occasionalkneaded appearance and slickensided surfaces in various shale units of
the Abo.
Strong jointing, often noted in the arkose lenses, probably is due tocompaction, gentle folding, and sympathetic breaking parallel to or enechelon with larger fault structures. Locally, the joints have had considerable influence on the distribution of mineralization, as subsequently described. Until the acetic acid-potassium iodide method of
identifying oxidized lead minerals was employed, the effect of joints inlocalizing deposition of copper carbonates was more obvious than was
their control of lead distribution.

Mineral Deposits
PRODUCTION
Lasky and Wootton (1933) estimate the production of the Sacramento district through 1931 as 1,600,000 pounds of lead and 100,000
pounds of copper. The data from which these figures are derived arefragmentary, but an independent check of Mineral Resources volumes
from 1900 through 1931 indicates their estimate is so close as to require
no further comment.
Since 1931, production has been reported in the Minerals Yearbooks.
Adding the figures from 1932 through 1962 to Lasky and Wootton's estimate gives an approximate production for the period 1908-1962 of
1,915,500 pounds of lead and 260,570 pounds of copper. Only minor
amounts of silver and gold have been produced.
Comparison of the pounds of metal produced with tonnage reported
since 1932 shows that the ore has been of two classes and that the grade
has varied as follows:
Lead ore
Copper ore

5.0 per cent to 11.0 per cent lead
2.0 per cent to 7.0 per cent copper

Private figures on production before 1932 indicate that much of the leadore averaged between 12 and 15 per cent lead, a quality possibly due inpart to hand-sorting.
Careful consideration of available figures for pounds produced andgrade suggests that total tonnages for the district could not exceed 23,000
tons of lead ore and 6500 tons of copper ore. Although at least ten othermines are mentioned in the history of the district, the bulk of the copperore has come from the Courtney mine and practically all the lead ore hascome from the Alamo mine. By 1948, the latter had come to be known as
the Warnock mine, after one of its former operators.

LEAD

MINERALIZATION

Lead mineralization in the Sacramento Mountains apparently is
confined to arkose beds within the Abo from Red Hill south to the Ady
mine. Although minor lead occasionally is found in several such beds, in a
specific area the principal values always are confined to a single light grayto yellowish cream arkose bed. This is well demonstrated by assay resultson random samples selected over the entire district from favorableappearing arkoses and by results of detailed sampling in areas ofinteresting mineralization. Where concentrated, the lead minerals may

12

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

make irregular, narrow shoots up to 25,000 tons averaging about 7 percent lead, although values may range from a trace up to 20 per cent. The
thickness of the ore shoots seldom reaches the full thickness of thearkose host beds which average less than 10 feet.
Lead may be represented by galena, cerussite, minor anglesite, or all
three; usually the higher values are in cerussite. These minerals, occurring together or separately, are disseminated between feldspar andquartz grains of the arkose, apparently at the expense of cementing
material. What probably is cerussite occasionally can be detected in clay
galls by the KI method. Rarely, cerussite can be observed on fracture
or joint planes.
Though frequently confused underground with fine-grained bluishquartz, galena usually can be recognized easily. Cerussite, however, blendswith altered plagioclase feldspars and carbonate cement so well that it isalmost impossible to detect. Galena frequently does not show on
outcrops, apparently having been leached. Often the leached surfaces are
exceedingly porous and have a dull gray appearance due to cerussite
and/or anglesite. Lead mineralization occasionally can be detected bycareful work with a pick and the use of KI on narrow limonite-stained
bands that may or may not show cerussite.
COPPER

Copper mineralization, characterized as the "Red Bed" type andconceded by some to be syngenetic originally but partly redistributed andreconcentrated by ground water in a second, epigenetic stage (Finch,
1933; Lindgren, Graton, and Gordon, 1910, p. 78-79), is widespread,though of minor commercial value, in the Abo Formation of the Sacramento Mountains. Copper concentrations usually are found in thesame general area with lead but also are known in a number of places
where significant lead has not yet been proved. Copper minerals may
predominate in beds above or below those containing lead or may occur
in the lead-bearing beds. Only at the Warnock mine, however, were reltively high copper values frequently found in conjunction with high leadvalues. In no place do the values of the two metals bear any consistent
relation to each other. Where an arkose bed occasionally is hereinreferred to as a copper bed or as a lead bed, it is intended to imply only thatthe indicated metal predominates.
In addition to being almost geographically coextensive with leadshowings, copper of the "Red Bed" type is known on the Mescalero
Indian Reservation north of Red Hill, on the southeast side of Ortega
Peak, and from several areas a few miles south of the Ady mine. It is also
known in the Tularosa or Bent district, but geologic relationships there
are different from those in the High Rolls area, and the Tularosamineralization may be of other than "Red Bed" origin (Lindgren,

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

13

Graton, and Gordon, p. 187-190). The copper concentrations usually are
narrow, small, and spotty, never more than several thousand tons being
extracted from a single locality.
The copper minerals in relative order of abundance are malachite,azurite, chalcocite, and chalcopyrite. The last two minerals often areassociated with pyrite or marcasite but rarely with each other.
Chalcocite may be present as nodular masses or as replacements ofwoody material or thin coal seams enclosed in sandy shale or shalyarkose. On Red Hill, north of High Rolls, chalcocite is disseminated ina thin, dense, light gray arkose bed. Chalcopyrite usually is present as
fine disseminations in the same general environment as lead but indetail commonly is segregated within the lead-bearing beds and isspecifically marked by individual iron-stained bands further colored byminutely disseminated malachite.
Malachite and azurite appear to have been derived from chalcocite
and chalcopyrite and probably represent fairly recent oxidation. Theyeither are associated directly with copper sulfides or have migrated awayfrom them, occurring as coatings and disseminations along bedding
planes and as fillings of fractures. Usually the occasional high copper
values in lead beds are due to these secondary carbonates.
Limited shipments of sorted ore have been made; in general, these
averaged slightly under 3 per cent copper. Copper assays of samples collected for this district appraisal occasionally have ranged up to 10 per
cent.
OTHER MINERALS

Iron is present in limonite, hematite, pyrite, marcasite, and magnetite.
Hematite is represented as staining in the sedimentary rocks. Magnetite
occurs as microscopic grains in the arkose. Pyrite and/or marcasite
frequently are found with nodular chalcocite, as mentioned above, andare in the lead beds usually as richly disseminated, irregularly circularspots. The former presence of pyrite is suspected in many localities fromdark brown limonite spots with peculiar gummy cores. This particularlimonite should be differentiated from the light to medium brownspotting or staining that may reflect migration of iron from a number ofpossible sources. Spots of the former type occasionally appear to be fairguides to concentrations of lead or copper.
In addition to the lead, copper, and iron minerals described, othermetals found in the Abo lead beds include zinc in the forms of smithsonite and cobaltiferous smithsonite (no sphalerite has been observed),
silver in unidentified minerals, vanadium in vanadinite, and vanadium andcopper in combination as rare cupriferous vanadates. Zinc is fairly
common in certain lead beds, though it seldom exceeds 0.1 per cent except in areas where its minerals are obvious on joint surfaces. Silver

14

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

rarely assays as much as 0.1 ounce, but it is quite persistent as a trace metal.
A sample taken in the Warnock area gave 0.4 per cent vanadium; thecupriferous vanadates locally displayed were not observed elsewhere in the
district.
Nine samples collected from the Tony, Dollins, Courtney, Black
Bear, Warnock, and Ady workings were tested spectrographically at the
New Jersey Zinc Company's laboratory and a check was made with aGeiger counter for uranium content. Amounts of metals of possible
interest, other than lead and copper, ranged as follows:
Zinc, 0.01 to 1 per centSilver, 0.001 to 0.01 ounce
Vanadium, 0.0001 to 0.01 per centTungsten, less than 0.001 per centCadmium, less than 0.001 per centManganese, 0.01 to 0.1 per centMercury, less than 0.001 per cent
Nickel, less than 0.001 per cent Tin,less than 0.001 per cent
Molybdenum, 0.0001 per cent or less
Uranium oxide, less than 0.01 per centBecause of the limited number of samples, these results are not conclusive but do suggest probable contents of these metals in the arkose
beds.
MINES AND PROSPECTS
Since the Warnock mine area has the most extensive showings of leadand consequently the most concentrated development, results obtained
there are especially pertinent when considering mineralization in otherparts of the district. For this reason, the Warnock appears first in thefollowing descriptions. Thereafter, areas are described geographicallybeginning with Red Hill at the extreme north end of the district andproceeding southward to the Ady mine. One digression is made from thisscheme to discuss mineralization in Karr Canyon.
WARNOCK AREA
In 1949, the Warnock mine area was covered by twelve unpatented
Alamo Extension claims owned by Frank J. Holmes of Modesto, California.
Development consisted of several thousand feet of drifts, inclines, stopes,
raises, open cuts, and short adits and 1550 feet of bulldozer work along thearkose member of the Abo.
Two lead ore bodies containing galena, cerussite, and minor anglesite
have been exploited from one general level of lenticular arkose beds.

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

15

Oxidized copper minerals, with malachite greatly predominating, arefound in shaly arkose above the lead-bearing arkose; these sameminerals are found as disseminations and fracture fillings within the leadbed. Chalcocite has not been recognized, and chalcopyrite is of rareoccurrence. Other minerals of restricted distribution include pyrite,
smithsonite, cobaltiferous smithsonite, vanadinite, and certain
cupriferous vanadates.
Geology
The Abo Formation in the Warnock area is shown on Plate 4. The
Abo rests in some places conformably and in other places unconformablyon the Magdalena. It attains a maximum thickness of more than 400 feetin the basin east of the main workings. The basal limestone conglomerate
member is thickest in this basin but thins gradually on the flanks andfinally disappears to the east and to the west. The arkose member ispersistent and varies from 200 to 300 feet in thickness. The red shalecapping member shows an apparent variation of 100 to 200 feet.
The basal conglomerate evidently represents initial erosional products shed from an early Permian land mass. The conglomerate phase
was succeeded by the alternate deposition of coarse sediment and finesilt, as might develop at mouths of large rivers during periods ofalternating flood and quiescence. Such relationships also are suggestiveof fan deposits. Finally, the only material reaching the basin was fine andappears to have been deposited under rather quiet conditions, resulting
in the ferruginous, arenaceous capping shales. It is possible that the
Warnock—Speckled Bird basin was once coextensive with that in the
Alamo Canyon—Stark Nose area. At least, the latter basin resembles theformer in its history.
Along the southern slopes, outcrops are numerous and the various
parts of the arkose member can be separated. Chocolate- and lightchocolate-colored arkoses can be traced by float blocks and outcrops forseveral hundred feet in some instances, but usually these may graduallyfade into cream arkose or become indistinguishable in the float. Shalewithin the arkose member is obscured by surface debris, but underground workings and bulldozer work indicate a ratio of about 60 per centshale to 40 per cent arkose. Small but economic concentrations of leadare confined to cream arkose lenses lying from 50 to 100 feetstratigraphically above the basal conglomerate.
The Warnock lead bed disappears under float to the northwest andpinches out in shale to the east. Direct correlation with the east Warnock
bed is prevented by the fault which has dropped the Warnock block
about 200 feet (down to the west), but the east Warnock bed is at thesame general level in the arkose member as that in the main Warnock

16

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

mine and probably is its equivalent. The east Warnock bed strikes east,
dips from 5 to 15 degrees north and varies from 4 to 8 feet in thickness.
It is strongly jointed with north- and east-trending sets predominating.
The bed lenses into shale east of the portal below point 1 on Plate 4. It
was bulldozer-stripped westward to point 4 where the great number andlarge sizes of arkose blocks and the steep hillside made further stripping
impractical. From points 1 to 2, this bed has a consistent thickness ofabout 6 feet, then it thins at 2 and interleaves with shale for about 40 feetwestward to the gulch. Southwestward from the gulch, it averages about
8 feet thick for 200 feet to point 3 where it becomes thin-bedded, shaly,
and chocolate-colored. Between points 3 and 4, it is poorly exposed andshaly, but at point 4, it is about 5 feet thick and cream in color. It
gradually lenses out westward toward the Warnock fault.
Since strike and dip observations in the Abo and in the Magdalena arerather well distributed on Plate 4, a detailed description of theirconsiderable variation is not necessary. Apparently the variations are due
to basin topography, sedimentation, and deformation. Slight folding has
in many instances produced northeast and northwest joint sets which
seem to have effected localization of lead and copper minerals.
The largest fault involving the Abo cuts through the Warnock area
about parallel to the Alamo Peak fault to the west (not shown). The
Warnock fault apparently has had a slight scissor or couple movementwith the greatest displacement of about 200 feet to the south. It is detectable mainly through discrepancies in positions of the red shale-arkose andarkose-conglomerate contacts. Also, the sharp change in dips of the
Magdalena limestones plus the abrupt disappearance of a distinctive
crinoidal limestone in the Magdalena as the fault is crossed suggest its
presence. A bulldozer cut on the fault at point 5 (pl. 4) discloses a yellow
zone, 6 feet wide, of shattered shales flanked on the west by red shales
and on the east by chocolate shales typical of those in the arkose member.
No mineralization shows in or near this zone, and the only alteration isslight bleaching and hardening of the red shales. The bleaching may be
due either to surface waters which have used the fault as a channel or tohydrothermal action; however, the Magdalena limestones are neither
altered nor mineralized on or near this fault.
West of point 2, just above the lead bed, is an old spring deposit ofgray travertine and calcareous tufa, suggesting that there has been considerable movement of ground water in the arkose member. Similar deposits occur in arkose on the northeast side of the Speckled Bird Nose.
On the western edge of the map area, an andesite sill with laccolithic
tendencies is present in the Magdalena limestone. It shows variation in
grain size due to chilling along its borders. No alteration occurs in the sillor in adjacent rocks. In the general area of the sill, a silty arkose bed
between Magdalena limestones and the basal conglomerate of the Abo

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

17

reflects the change in late Pennsylvanian from marine to continental
conditions of sedimentation.
Southeast of the sill is a pre-Abo normal fault with 50 to 100 feet ofdisplacement, down to the east.
Sampling Results
All arkose outcrops were tested with KI and the results recorded on
Plate 5. The only areas showing favorable response were those outcrops
near the main Warnock mine portal and those at the east Warnock workings. Most of the cuts and likely outcrops were sampled and assayed withresults comparable to those of the KI test, the only appreciable values
being found in the two areas just mentioned.
The strip of arkose exposed by the bulldozer in the east Warnock area
was sampled and tested with KI; the results are shown on Plate 6. KI
tests suggest two possible concentrations of lead. One extends from the
Alamo No. 1 adit, point 1, westward about 200 feet. The second extends
from the gulch, at the break in the section, southwestward for 300 feetwhere the bed begins to finger out into shale. Lead assays showinteresting variations within short distances. In the first concentration,
two high-grade samples containing 14.70 and 17.10 per cent lead wereobtained from 2 feet of the bed. Assay of an adjacent sample, HR-404,
showed 0.55 per cent lead, and values dropped to a trace of lead insample HR-405 at the lower Warnock No. 2 portal. In the second "concentration," lead values do not exceed 0.15 per cent, being no better orworse than those in supposedly barren parts of the bed.
In all samples from the bulldozer cut, other metals followed theirusual patterns. Silver ranged from a trace to 0.26 ounce (higher values
were with higher lead assays), copper from 0.06 to 0.66 per cent, and zincfrom a trace to 0.15 per cent.
Warnock Mine
Three plates are included to illustrate the geology of the Warnockmine. Plate 7 is a plan of the mine with certain selected sections to which
the generalized results of sampling and KI work have been added. All
underground workings were sampled at about 20-foot intervals or less;results are recorded on Plate 8. The sample points then were treated with
KI and any adjacent areas of interest also were tested. The red coloringon the plan (pl. 7) represents appreciable KI results, while red on the
cross sections represents tentative ore shoots as outlined by assay results
and defined more precisely by KI work. Plate 9 is a block diagram
showing underground workings, geology, and distribution of galena
within the arkose bed.
The lensing into shale and the swelling of the arkose bed are clearlyshown in the plan, sections, and block diagram. The bed grades into

18

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

shale in almost every direction but west and possibly a narrow strip to
the northeast. The long axes of its thicker sections show slight orientation parallel to the dip, but such sections commonly are featureless as far
as sedimentary structures are concerned. Where the bed begins to thinout into shale, bedding planes break up its massive appearance. In thevicinity of points 1 and 2 on Plate 7, the arkose is strongly cross-bedded
in a manner suggesting swift scouring currents of changing paths. It isnoteworthy that at these two locations, the lead carbonate ore shoots, as
outlined on section D-D', seem to truncate in horizontal ends that areparallel to the foreset limbs of the cross-bedding as if the mineralizing
agent were traveling down dip and became diverted to the hanging wallby the horizontal laminations. These near-horizontal shoots in a bed
dipping 15 degrees suggest a series of level bubbles. This effect also is
illustrated by section C-C'.
Jointing and fracturing in the Warnock bed are represented by two
main trends; northwest, parallel to the strike of the bedding, and northeast, parallel to its dip. The ore shoots are aligned subparallel to the dip
set of joints, although the strike set is the more prominent. The joints
usually do not penetrate the shales above or below the arkose. Almost allof them are open and smooth-surfaced. Both sets of joints may havebeen produced by settling and flexing of the arkose with the adjacentincompetent beds adjusting to the forces by flow and bedding planeslippage.
In the over-all picture, individual joints do not seem to have controlled lead distribution, although a possible relation is suggested by thefact that mineralization is coincident with zones of concentrated
jointing. In detail, however, the joints have definitely effected concentration of lead carbonate, but they exert no apparent effect on galena
distribution. Galena commonly is in discontinuous ribbons which range,
without obvious reason, from top to bottom of the arkose bed, but concentrations of this sulfide occasionally do show relation to the details ofcross-bedding.
Three graphic examples of the influence of joints on lead carbonate
distribution, as revealed by KI work, are shown in large scale on Plate 7.
These are from parts of stope walls that were sprayed with KI. In someinstances, however, the distribution of values has not been controlled byjoints at all. In only a few instances in the mine are joint faces coatedwith lead carbonate, even when adjacent wall rock is heavily impregnated with it. This suggests that the fractures acted more as dams to themineralizer than as channels for it. The concentration of lead carbonate
on the up-dip side of the joints wherever noted suggests a possibility
that the lead-bearing solution traveled down dip, was backed up at joints
whose surfaces are smooth and much less permeable than normal
arkose, and deposited its load behind these faces.

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

19

East War no ck Wo r kings
Galena is visibly disseminated in small shoots underground in the
East Warnock arkose bed. Limited KI tests indicate the presence of
cerussite. Possibly 2000 tons of ore averaging about 6 per cent lead havebeen mined from the several hundred feet of workings. Geology andassay results are presented on Plate 10.
RED HILL

That area designated as Red Hill is less than a mile north of High Rolls on
the eastern half of property owned in 1949 by Allan Walker of Alamogordo,
New Mexico (pl. 3).
Red Hill has a cap of Yeso limestone, is comprised almost entirely of
the relatively flat-lying Abo arkose member, and is underlain by Magdalena limestone. The basal conglomerate member of the Abo is unlikethat to the south, being composed almost entirely of well-rounded
quartzite and chert pebbles up to 6 inches in diameter in both calcareousand quartzose matrices. The arkose member is similar to that farther
south except that purplish arkose beds are more abundant. These occasionally range up to 15 feet in thickness and alternate with red or
purple arenaceous shale bands. An arkose bed near the base of the member changes in color laterally from cream to purple and, though averaging about 6 feet thick, occasionally ranges up to 12 feet. The main
purple beds occasionally show mottled bleaching, an effect which
probably results from the action of ground waters moving in porous beds
and along joint planes. All arkose beds are characterized by abrupt
lensing. Other than local north- and east-trending joint sets, limited toarkose, no structure is evident.
The best known mineralization is low-grade copper carbonates in athin, gray, arkosic shale seam in the lower part of the Abo arkose member
near the base of Red Hill. The carbonates replace organic material liketwigs and leaves and coat intergranular spaces, joints, and bedding planes.
This mineralization is developed by a few short open cuts on the east andwest sides of Red Hill.
In addition to the copper carbonates, fine blebs and erratic stringers
of chalcocite occur in a thin, dense, cream arkose bed high in the
arkose member on the northeast side of Red Hill. Sparse malachite also
is present, but because of the dense character of the rock, oxidation has
been inhibited.
"Red bed" type of copper showings are known both east and north of Red
Hill but were not examined by us.
A cream-colored bed near the base of the Abo arkose member on thewest side of Red Hill contains one restricted area of zinc-lead mineralization. Visible galena, slightly oxidized to cerussite, is disseminated20 NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES
over a width of 2 to 6 inches and appears as fine blebs in other partsof the rock. Mineralization in the bed responded poorly to the KI test.
The arkose is cut by joints that do not persist beyond its 6-foot thickness. The sample results are presented on Plate 11. The higher zincvalues are in botryoidal smithsonite on or near joint planes, while several samples of compact, unfractured rock uniformly assayed 0.10 per
cent zinc. These relationships suggest that zinc may have been leachedfrom a considerable area and concentrated in the joint channels byground waters.
SACRAMENTO GULCH AREA

Showings of lead and copper in the vicinity of Sacramento Gulch,about one mile southeast of High Rolls, in 1949 were covered largely by
twelve unpatented claims. These were owned by M. F. Drunzer of High
Rolls and R. S. Casner of El Paso, Texas. Some of the better mineralization is on the Dollins homestead directly east of the unpatented property(pl. 3).
Surface and subsurface geology and assay results are illustrated on
Plates 12 and 13.
The sub-Abo Magdalena Group is in angular unconformity with theAbo. The Magdalena beds strike northwest and dip from 5° to 40° NE.
The overlying Yeso appears to be disconformable, but this appearance
probably is created by float blocks spilling across the contact. Neither the
Magdalena nor the Yeso shows evidence of mineralization.
Nearly half this area is covered by Yeso float; consequently, only
about 200 feet of Abo are exposed at any locality. Except for two places
in Sacramento Gulch, neither basal conglomerate nor red shale is exposed, the main rock type being arkose. Thick surface cover made it
impossible to separate the arkose member into units for correlation, but
an attempt was made to trace arkose beds that cropped out and obtainsome idea of the structure. This work indicated that the arkose unit
bearing lead in Sacramento Gulch is in the same relative stratigraphic
position as the bed developed by the Tony tunnels about 50 to 75 feetabove the base of the Abo. This stratigraphic position of productive
arkoses is comparable to that in the Warnock area.
The combination of surface and underground mapping proves thearkose beds are lenticular. Diastems plus general lensing result in thickness ranges of from 0 to 15 feet. Diastems are well developed in the vicinity of the Dollins tunnel, Sacramento open cut, East Sacramento No.
2 tunnel, and Tony tunnels; exposures in the East Sacramento No. 2
tunnel suggest that all channels are separate entities and may have preferred orientations of about N. 45° E. In nearly all instances here andoccasionally elsewhere, galena, chalcopyrite, copper carbonates, andjointing are almost coextensive with thicker parts of the channels.

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

21

Practically all the main workings show more or less galena disseminated in a cream arkose bed. Cerussite usually occurs with galena at
the outcrop but gradually or rapidly fades with increasing distancefrom the surface. Occasional clay galls which show no galena but
which respond very well to the application of KI suggest absorptionof lead carbonate.
Copper is represented principally by malachite, commonly disseminated with lead values in the arkose; it occasionally appears in beds otherthan those bearing lead. Chalcopyrite occurs in the arkose at the Dollins
tunnel but also is in a narrow limonite- and malachite-stained bandexclusive of lead minerals. Pyrite is visible in the East Sacramento No. 2
tunnel.
Development in this area comprises about 500 feet. The Dollins
workings investigate lead mineralization in a 10-foot-thick section ofarkose. The headings expose two main joint sets; the predominant set
strikes northeast, the other, northwest. Most of these joints are filled withrubble and dirt from the surface which is about 15 feet above the back.
The arkose is cream, coarse, and contains several small, gray shale pods.
A 1-inch shale seam and other bedding features indicate a dip of about
10° NW. At the end of the east drift, chocolate-colored shale in the floor
presumably represents the footwall of the arkose bed.
The east drift shows a large amount of easily visible but scatteredgalena and rare chalcopyrite, particularly in the upper half, but the
response to KI was slight. The galena imparts a high-grade appearance
to the arkose, but most of the assay values are low because of thepaucity of lead carbonate. Some relatively high assays, however, wereobtained along several feet of the east wall near the back. Galena,
although apparently concentrated in strongly jointed or fractured areas,is unrelated to such areas in its detailed distribution; sedimentaryfeatures such as deeper parts of channels, porosity, and cross-bedding
provide the detailed control. The probability is that a joint plane will
have no more disseminated galena on its face than will arkose inches orfeet from such a plane. As demonstrated at the Warnock, this is nottrue of lead reconcentrated as lead carbonate; the joints may serve as
dams but only rarely as channels. At the Dollins workings, leadcarbonate is scarce except in outcrop.
The North Sacramento adit is driven in red shale, the lead-bearing
arkose horizon being the back. The base of the arkose is marked by ascab of disseminated galena and cerussite which ranges up to 3 inches inthickness. A sample selected from this band and including some arkose
above it assayed 0.03 per cent copper, 3.38 per cent lead, and 0.42 percent zinc. The Sacramento open cut, adjacent to the tunnel, exposes thefull width of the lead bed; the sample cut over the 7 feet of width
assayed 0.04 per cent copper and 0.75 per cent lead. KI results were
uniformly poor.

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NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

The cut reveals spots of fine-grained galena erratically and sparsely
distributed over the face. The lower 6 inches of bed, corresponding tothat in the back of the North Sacramento adit, show a concentration ofgalena and a favorable reaction to KI.
LOWER KARR CANYON

The geological environment in lower Karr Canyon (pl. 3) is merely thesoutheasterly extension of that in the Sacramento Gulch area (pl. 12)
except that more Abo red shale is found in Karr Canyon. Valley fillobscures the lower part of the Abo arkose member and the underlying
Magdalena Group. The Yeso Formation shows its usual irregular relations with Abo red shale; Yeso float occasionally obscures the shalecompletely and is in contact with the arkose member. Cover is so thickthat continuity of beds and structure are difficult to establish. However,
the arkose member seems to be persistent and its individual arkose beds
relatively flat-lying and characteristically lenticular.
Two undeveloped spots of mineralization occur in jointed creamarkose beds on the southwest side of Karr Canyon. One showing ofslightly disseminated malachite is of little more than passing interest: theother is slightly oxidized galena, finely disseminated in thin, irregular,
limonite-stained bands. Samples of the best showing of lead assayedpoorly. A limited KI test over the exposed parts of the bed indicated noreconcentration of lead as cerussite.
Arkose beds prominently exposed along the east side of Karr Canyon
have been visually examined and KI-tested in part. They appear to be
totally lacking in metal values of any kind. The beds are predominantly
purple in color but are believed to be equivalent in part to favorableappearing but mostly barren cream-colored beds on the west side of thecanyon. Extensive deposits of calcareous tufa are concentrated at themouths of several small gulches.
SACRAMENTO GULCH TO COURTNEY MINE

Between Sacramento Gulch and the Courtney mine, only minor
showings of base metals are to be found in the Valley, Stream, Coachman, and Cactus cuts, approximately located on Plate 3. The two
small Valley cuts expose slightly oxidized galena associated withlimonite and malachite disseminated in a thin, cream arkose bed abovethat usually bearing lead.
The Stream adit develops a cream arkose below the bed exposed by
the Valley cuts; the "Stream arkose" also is higher in the section than the
arkose bearing lead in Sacramento Gulch. Although no lead can be seen
underground, some galena ore is piled on the dump. Samples from thetunnel assayed no copper and only sparse lead.

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

23

Lead was faintly indicated by KI tests in the Coachman and Valley
cuts.
COURTNEY MINE

Three unpatented claims, the Grandview, Courtney No. 1, andCourtney No. 2, control all showings of copper and lead in and near the
Courtney mine. In 1949, F. E. Calkins of High Rolls owned these claims(pl. 3).
To date, only copper ore has been produced from a surface open cut
and from inaccessible underground workings. Mining has been limited toa contorted, much fractured, shaly arkose stratum containing nodules ofchalcocite and copper carbonates. During the early history of theproperty, the mineralized arkose was mined and allowed to disintegrateon the surface; the chalcocite and copper carbonate nodules then werescreened out and shipped. In later years, some production has come fromlower grade copper carbonate which impregnated shaly arkose and replaced fossil twigs and leaves within it.
An inaccessible 90-foot shaft in the open cut reputedly encounteredan arkose stratum about 50 feet from the surface. A limited explorationof the bed disclosed thin streaks of fairly high-grade galena. What probably is the same bed crops out about 200 feet west of the shaft. This
cream arkose has been investigated by trenching, jackhammer holes, andshallow shafts, but only minutely and sparsely disseminated galena andcerussite have been found. Assay results are reported on Plate 14.
COURTNEY MINE TO ARCENTE CANYONThis section of ground shows more structural complexity than any
other in the district (pl. 3). As a consequence, there is exposed in Arcente
Canyon, with varying degrees of conformity, sediments ranging from theOrdovician El Paso Limestone to the Permian Yeso Formation. Becauseof irregularities in sedimentation, the Abo is represented by varying
thicknesses of its arkose and red shale members. On the south side ofArcente Canyon, the Abo Formation rests directly on Mississippian
crinoidal limestones.
Several of the fault structures shown are pre-Abo in origin and possibly are related to the evolution of the ancestral Rockies; others involving the entire exposed section possibly are of Laramide age. Some earlyfaults may have been reopened by later stresses. Because of the combined
effects of at least two orogenic periods, strikes and dips of beds in all
formations are quite irregular.
The few mine workings expose galena and its oxidized productsslightly disseminated in a cream-colored arkose bed. These showings arein the Black Bear and Andy open cuts on the north side of Arcente

24

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

Canyon and in the Bisbee adits located on a tributary gulch on the south
side of the canyon. In 1949, the Black Bear unpatented claim was owned
by F. E. Calkins. Assay results for the Black Bear are on Plate 15; thoserelating to the several Bisbee workings are on Plate 16.
SPECKLED BIRD NOSE

Sediments on the Speckled Bird Nose, the north continuation andthicker part of the basin of Abo sediments which contain the Warnockmine, have been described under the Warnock. One easterly trending
fault, subparallel to one in Arcente Canyon and to one directly south of
the Courtney mine, was mapped (pl. 3).
Thick Abo in the basin is connected by a thin veneer of arkose andred shale to the same members in Arcente Canyon. No mineralization is
known in this thin strip, although several arkose fragments with poorcopper showings were found near the forest road.
On the west side of the main nose, minor showings of malachite,azurite, and chalcocite in a fractured, massive, lenticular, cream arkose
bed have been developed by several short adits. Travertine locally isabundant on joint surfaces. Limited KI work on various parts of the explored bed failed to indicate lead carbonate, and no galena was recognized. Similar results were obtained from a lower arkose bed.
Two miles due west of the Speckled Bird Nose on the southwest sideof Ortega Peak, scanty disseminations of malachite and azurite were reported by A. L. Bowsher (personal communication, 1948).
WARNOCK EXTENSION TO ADY MINE

Adjoining the Alamo Extension claims (Warnock) on the east andcovering the outcrop of Abo arkose beds to Caballero Canyon were thethree unpatented claims, Warnock Extension Nos. 1 and 2 and Caballero
Extension No. 1 (pl. 3), owned in 1949 by M. F. Drunzer of High Rolls.
Excellent exposures in Caballero Canyon show structure in the Magdalena Group to include anticlines, synclines, and block faults, all ofwhich predate deposition of the Abo. Partly because of the irregularities
on the eroded Magdalena surface and partly because of sliding of the incompetent Yeso rocks across the contact, the Abo appears to vary greatly
in thickness. The three members of the Abo are presented, but the basal
conglomerate and the red shale show surface discontinuity because of
conditions just described. The arkose member is persistent though occasionally obscured by slide blocks of the red shale member.
Structure in the Abo is reasonably simple. The northwest-striking
monocline is very gently warped by both strike and dip anticlines, synclines, and terraces. Northeast and northwest joints or fractures often
appear to be localized by these gentle folds. Geology and assay results ofworkings in this area are shown on Plate 17. Malachite and galena are

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

25

found separately and together in cream-colored arkose beds of marked
lenticularity. Because of good exposures, all signs of mineralization havebeen given some attention in the past. Although rumors exist of numerous burro loads of high-grade copper ore having been packed out fromthe Bueno mine (never positively located by us), it is believed that
production from this area could not exceed a few hundred tons of lowgrade ore.
West of the road, several float blocks of cream arkose containing
spots of malachite and heavily disseminated, somewhat oxidized, galena
are found. Specimens from this locality are interesting in that cubic casts
suggest that galena can be leached from arkose in a limited way without
residual cerussite or anglesite forming. Such casts also might result fromthe leaching of pyrite without the formation of residual limonite.
On the dump of a caved cut at the northeast corner of Warnock Extension No. 2 are blocks of arkose with richly disseminated galena, but
no ore has been proved in place. These blocks possibly represent material
selected from the float by prospectors.
Except for one small cluster of pyrite crystals, no sulfide has beenfound in the Magdalena limestones.
ADY MINE AREA

The Abo rests with marked angular relationship on the Magdalena
Group and may be partly disconformable with the Yeso Formation. The
Abo, about 200 feet thick, is represented by nearly equal amounts of thearkose and red shale members. Strikes of beds within the Abo are about
N. 30° W.; dips vary up to 25° NE. No faults were found (pl. 3). One
hundred feet of open cut and several hundred feet of irregular inclined
workings investigate showings of malachite, azurite, and chalcocite (see pl.
18). These minerals have replaced carbonaceous material and have been
deposited in joints and bedding planes in a somewhat shaly bed of arkose
10 feet thick, about 50 feet above the Abo—Magdalena contact. The
general environment of the copper resembles that at the Courtney mineand that on the Speckled Bird Nose. Fifty feet above the copper-bearing
bed, four short irregular inclines are driven on a cream arkose stratum
about 7 feet thick. In general these workings showed poor assays, but in
one incline lead carbonate ore, with no visible galena, assayed up to 11
per cent lead over a width of 5 feet, and copper values up to about 3 percent also were indicated.
The most extensive working in the Ady area is a 15-degree incline reported to be 1800 feet in length but now badly caved and partly inaccessible. Though predominantly in red shale of the arkose member, thisincline cuts several arkose strata, including one bearing lead. Lensing of
the arkose beds shows well in the incline, but no galena or cerussite isevident.

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NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

About 500 feet down the incline from the portal, malachite occurs ina coaly seam interbedded with red shale and ranging up to 6 inches inthickness. In a southeast crosscut, a few hundred feet farther down thedip, a 4-inch band of nodular chalcocite and pyrite, often mutually intergrown and brilliantly coated with malachite, can be seen in what probably
is the same thin coal band.
South of the Ady mine only slight copper mineralization has been
revealed in the Juniper cuts. No mineralization is known on Stark Nose
southwest of the Juniper showings.
ORE GENESIS
Information on the Sacramento district pertinent to a discussion ofgenesis of the several ore types is summarized below:
1. No clear evidence of hydrothermal action is known in any of theformational units either above or below the Abo Formation from northof High Rolls south to Alamo Canyon. Structures either crosscutting theentire sedimentary series or confined to a limited stratigraphic section
show no mineralization or alteration.
2. Andesite sills and dikes occur in or near the district. No
significant alteration is found adjacent to them. No intermediate intrusive
rock types, such as quartz-monzonite, are known.
3. Lead occurs in galena and cerussite and rarely in anglesite. In detail, the first two minerals may occur together as cerussite coating galena
or as independent but often closely associated disseminations. Anglesite,when present, always coats galena. Occasionally galena may be bunched
into patches and discontinuous stringers. These minerals often are associated with copper carbonates, chalcopyrite, pyrite, silver in unidentified minerals, and zinc, probably derived from sphalerite and reconcentrated as smithsonite. Cobalt and vanadium are of rare occurrence.
Copper in chalcocite, chalcopyrite, malachite, and azurite is found inseveral arkose and shale beds entirely within the Abo and may be associated with or independent of obvious lead mineralization. Chalcocite
commonly replaces carbonaceous materials and rarely appears as disseminations. The reverse is true of chalcopyrite. The copper carbonates
apparently have been derived from the sulfides and may appear as independent replacements of carbonaceous material, as disseminations, andas coatings on bedding and joint planes.
Pyrite or marcasite may be found in the same situations as the copper
sulfides.
4. The principal lead mineralization is at a fairly constant level in the
Abo arkose member in beds sandwiched between relatively impervious
shales.

SACRAMENTO (HIGH ROLLS) MINING DISTRICT

27

5. Minor lead values in the form of partly oxidized galena are rather
evenly distributed in the outcrop of the lead horizon over the entire district,but occasionally the metal appears in minor quantities in arkose beds at otherlevels.
6. Possible arkose host beds represent parts of ancient stream channels. These are highly lenticular, tending to grade rapidly into shale inalmost every direction. Often the arkose remnants are isolated, disklike
masses, not visibly tapped by faults.
7. No alteration or mineralization is evident in red shales or
possible feeding structures adjacent to the lead ore bodies, although bothlead and copper minerals show a tendency to occur in light-coloredarkose beds.
8. Galena concentrations, though frequently appearing in strongly
jointed arkose, bear no relation in detail to joint, fracture, or main
bedding planes. Galena seems more controlled by thicker channel positions and sedimentary features such as cross-bedding within these channels.
9. The long-exposed surfaces of certain specimens show cubic casts
suggesting complete leaching of galena with no formation of residual leadcarbonate or sulfate.
10. Spring deposits of several types reflect the activity of groundwaters.
11. Cerussite or cerussite-rich calcium carbonate rarely is found on open
joints. Smithsonite is not uncommon as a filling, but zinc sulfide has not beenrecognized.
12. Lead-carbonate concentrations commonly are found in coarser
parts of the arkose beds. These concentrations may terminate abruptly
down dip against joint surfaces or foreset beds of the cross-bedding andgradually fade out on the up-dip side of such surfaces. This produces whatmight be termed the "level bubble" effect at the Warnock mine wherelead-carbonate shoots have a near-horizontal attitude within an arkose bed
dipping 15 degrees. These shoots are arranged at six different
recognizable levels (pl. 7, section C-C').
13. Clay galls and seams within lead-bearing arkose occasionallyrespond well to the KI test and contain no visible galena.
DISCUSSION AND CONCLUSIONS

Disregarding the great number of geological factors involved atvarious times, the problem in genesis, as suggested by the evidence, canbe separated into two parts: first, the means by which the metals wereintroduced into the sediment and, second, the means by which they
were subsequently concentrated.

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NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES

As to the first, when we entered the district, we favored the view thatthe structural history, presence of igneous rocks, and assemblage ofmetals implied a hydrothermal origin for the ore deposits. As evidence
accumulated, we gradually began to favor a hypothesis of "semisyngenetic" origin.
Though the chemical factors involved may be somewhat different, thegeneral histories of the copper and lead mineralizations probably arealmost identical. Because of their frequent direct association with copperand lead, iron (subsequently deposited as pyrite), zinc, silver, vanadium,and cobalt must have been deposited by the same processes suggested
for copper and lead.
Our use of the term semisyngenetic (H. A. Schmitt, 1948, has coined theterm syngenoid for this type) implies that the sulfides, originally epigenetic
and hydrothermal in origin, or accessory minerals in igneous rocks, wereleached and carried as salts by surface and ground waters and to a lesser
degree as fine metalliferous detritus from sites of original emplacement
into basins of accumulating sediments. The metal salts may in part havebeen sulfidized by 1-1 2 S, possibly generated from decaying vegetable
matter, and trapped in porous unconsolidated arkoses and shaly arkoses
in the basin. Copper sulfides probably were deposited in shales byreduction of the soluble copper sulfate by organic material.
The first eight items summarized above, though indirect, tend tosupport this possibility for initial emplacement of the sulfides in the arkose. In addition, the continuous, lateral, far travel required for lowtemperature hydrothermal solutions moving through discontinuous
beds, with limited channels available, makes a hydrothermal origin
questionable.
As to the second part, there can be little doubt that most of thecopper carbonate in the district has resulted from fairly recent oxidationof original copper sulfide. That organic material was influential as aprecipitant is indicated by the common association of copper carbonate
with coal and well-preserved woody material.
The last five items summarized above strongly suggest that lead was
taken into solution by ground water, migrated to some extent, and was
redeposited as cerussite. During this ground-water phase and the later
period of oxidation, some cerussite and anglesite actually were fixed assurface coatings on galena. An immediate natural argument, because of
the usual nonmigration of lead under oxidizing conditions, is that thelead-carbonate concentrations have been derived from galena in place. In
counterargument, it can be pointed out that the KI work spectacularly
demonstrates, and the sodium sulfide test confirms, that slightly oxidized
galena and cerussite with no sulfide cores whatsoever often have mutual
boundaries. In such situations, galena commonly is disseminated, whilecerussite often occurs in irregular forms apparently developed at the expense of cementing material and controlled by the shape of feldspar andSACRAMENTO (HIGH ROLLS) MINING DISTRICT

29

quartz grain boundaries. The presence of lead carbonate in clay galls tothe exclusion of galena suggests absorption of lead salts from migrating
ground water.
The fact that lead and copper minerals tend to occur in light-coloredarkose beds suggests that the beds either were light-colored to begin withor have been leached to some extent by circulating ground waters. However, the same effect would be expected from circulating hydrothermal
solutions.
All this has led us to the conclusion that the ores in the Sacramento
district are "semisyngenetic" in origin and are confined to the Abo. It is aconclusion that stimulates interesting speculation as to the original sourceof the sulfide minerals, but this involves a regional geological problem
broader than could be covered during this project.

`references
Darton, N. H. (1928) "Red Beds" and associated formations in New Mexico, U.S.
Geol. Surv., Bull. 794, p. 198-220.
Finch, J. W. (1933) Sedimentary copper deposits of the western states, in Ore deposits of the western United States, Am. Inst. Min. Eng., Lindgren vol., p. 481 487.
Jerome, S. E. (1950) Special field applications of a confirmatory test for lead, Econ.
Geol., v. 45, p. 358-362.
Lasky, S. G., and Wootton, T. P. (1933) The metal resources of New Mexico and theireconomic features, N. Mex. Inst. Min. and Tech., State Bur. Mines and MineralRes., Bull. 7, p. 85-87.
Lindgren, Waldemar, Graton, L. C., and Gordon, C. H. (1910) The ore deposits of New
Mexico, U.S. Geol. Surv., Prof. Paper 68, p. 78-79,187-190.
Pray, L. C. (1961) Geology of the Sacramento Mountains escarpment, Otero County,
New Mexico, N. Mex. Inst. Min. and Tech., State Bur. Mines and Mineral Res.,
Bull. 35,144 p.
Schmitt, H. A. (1948) Proposed field classification of the mineral concentrations of
economic interest, unpub. ms., 11 p.