Member
Gypsum
ofYeso
Canas
(Permian)
in NewMexico
Formation
Northrop, 1946)has beencorrelatedwith the
De Chelly Sandstoneof the Fort Defiance,
Arizona, areaby Baars(1962).This mediumbedded, reddish-brown to light-tan, finegrainedsandstone
with interbedsof calcareous
and sandymudrocksis the most widelyrecogTenneco
Tucson,
AZ,
C.
OilCompany,
byJames
nizableand areally extensivememberof the
NM
Albuquerque,
Universityof
NewMexico,
V.
ll, Department
of Geology,
andRaymond
Yeso.Most of this member was depositedin
fluvial, flood-plain,and marginal-marineening the stratigraphyof the PermianSystemin vironments(Baars,1962).
Introduction
Mst',Issn-The Los
(1970),Baars
Los Vallos oR TORRES
Laminae in evaporites,such as those ob- centralNew Mexico: Anderson
Va{os (Kelleyand Wood, 1946)is character(1968),
Hayes
(1962),
and
Bachman
Bachman
Member
the
of
servedin the CafrasGypsum
(1958),Bachmanand Myers (1969),Black ized-by relativelythin (0.l-3.0 m) beds of
YesoFormation,have beeninterpretedas ba(1973),Dane and Bachman(1965),Headley limestone,dolostone, sandy or muddy red
yearly
formed
deposits
varves
cyclic
sinal
or
(1968),Johnson(1969),Kottlowski (1975)' beds, and gypsum. Complex facies changes
by seasonalblooms of planktic organisms
Kottlowski and Foster(1960),Kottlowski and occuron a scaleof kilometers,but no distinct
in
water
chemistry
seasonal
changes
and/or
define the boundariesof
(Deanand others, 1975).Depositsof laminar Stewart(1970),Kottlowski and others(1956), lithologic changes
this unit.
(1949).
and
Lloyd
relain
arid
climates
in
accumulate
evaporites
The Los Vallos appearsto havebeendeposThe geologichistoryand stratigraphyof the
tively still lagoons or bays with restricted
ited on a low, flat coastalplain, which periodmarineinlets (Schmalz,1969).A water depth study area have been reconstructedwith the
was submergedby brief marine transgreaterthan the maximumwavebaseis neces- aid of Cook and Bally (1975),Dott and Batten ically
Foster gressions.The percentageof carbonatesand
sary for the preservationof laminae. The (1981),Hock (1970),Kottlowskiand
(1960),Rocky Mountain Associationof Geol- evaporitesincreasesupsection,indicating an
Caflas evaporiteswere depositedin a late
(1979),and overall trend of rising sealevel, gradual subLeonardian(Baars, 1962)hypersalinelagoon ogists(1972),Stearnand others
(1961).
sidence,and/or lesseningof detrital input.
Thompson
with an area of approximately25,000 km'
Laminatedevaporiteshave beenstudiedin The culmination of this transgressivetrend
(fig. l). East-centralNew Mexico was an arid
Koopmans wasa relativelystablehighstandduring which
coastalplain and shorelinein Leonardiantime great detail by Anderson and
Memberwasdeposited.
(Dott and Batten,l98l), and the Caflaslagoon (1963),Andersonand others(1972),Deanand theCaflasGypsum
Gvpsulr MEMBER-Within the
(1975),
(1969),
Cnffns
Sloss
and
Schmalz
others
may representa relativelyshort-livedand shalpapersby studyarea,the CaflasGypsumMember(Needlow arm of the deepand persistentPermian (1953). Of particular interestare
(1967)
ham and Bates,1943)is definedas the stratiDzens-Litovskiy
Dzens-Litovskiy
and
seasto the southand east.
graphicallycontinuous,upper-middlegypsum
This paper relatesthe stratigraphyand pe- and Vasil'yev (1962)describingthe ongoing
and carbonatememberof the Yesoand generbay
of
in
a
restricted
deposition
evaporites
of
trology of the CaflasGypsumMember to the
ally consistsof a basal,laminated,dolomitic
Kara-Bogaz-Gol.
known
as
the
Caspian
Sea,
overall paleoenvironmentaland paleogeofor
limestonewhich is fetid, carbonaceous,and
model
actualistic
This
locality
serves
as
an
graphiccontextof Leonardiandepositsin cenlocally fossiliferous;a lower laminatedgypCaf,as
the
of
the
depositional
environment
tral New Mexico.The lateralextentand facies
sum unit 10-20m thick with somethin (0.1Member.
Gypsum
boundariesof the Caflaswere mappedon a
0.5
m) carbonatebeds; a continuousbed of
l:500,000base(fig. l), modifiedfrom Dane
Stratigraphy
to laminar, dolomitic limestone
thin-bedded
(1965).
Sourcesof information
and Bachman
(2-5
with thin (0.1-0.5m) gypsum
thick)
m
into
divided
The
Yeso
has
been
Formation
included field mapping (Hunter, 1980), inlaminated gypsum unit
an
upper
beds;
and
Sonear
four
members
at
the
type
section
(unformation from TennecoOil Company
(10-20
beds commonly
Sandstone
m
thick).
the
Blanca
Sandstone;
corro:
Meseta
the
basal
published report, 1979), and other sources
near its western
Caflas
interval
in
the
occur
Torres
carbonate,
Los
Vallos
or
lower-middle
petrographic
Iisted in fig. l. Samples for
analysiswere collectedfrom outcrops near evaporite,and sandstonemember;the upper- marglns.
Fig. I illustratesthe lateralextentand facies
middle Caflas Gypsum Member, which inEngleand Socorro.
and
cludessome carbonatesand sandstones;
the upper Joyita Member,which is composed
Previouswork
primarily of sandstonewith somecarbonates
ALSOIN THISISSUE:
Lee and Girty (1909) first describedand to the north and west and predominantlyof
stratapenetrated
EarlyTertiary(?)
to the southeast(figs. I and 2).
named the Yeso Formation in New Mexico. carbonates
in Jornadadel Muerto
P.53
Regional Yeso-lithofaciestrends typically
Needham and Bates (1943) redescribedthe
Uraniumresourcesin New
Mexico-discussion of the
Permian Systemand located and measured show gradationsfrom silty and sandy conN U R Ep r o g r a m
P.54
type sections.Regionalcorrelationsof Per- tinental red beds in the north and west into
p.59
OliverLee MemorialState Park
mian depositsof the ColoradoPlateauregion shallow-marinecarbonates,evaporites,and
p.61
Service/News
(1962),
These
IiDixon
have been compiledby Baars
sandstones
in central New Mexico.
p.64
I n d e xt o v o l u m e3
(1967),and Skinner (1946).Discussions
of carboof
thologiesgradeinto a thick sequence
in
New
correlative
Permianstratigraphy central
Mexico nates to the east and southeast,
SOON
COMING
may be found in Andersonand others(1972), with the Bone SpringsFormation of eastern
of
EoceneBaca
sediments
Lacustrine
Bachmanand Hayes (1958),Kottlowski and
NewMexicoand westTexas(Skinner,1946).
Formation
Stewart(1970),andSpeed(1958).
MEsEta BleNce SeNostoNe MnvsnnButteStatePark
Elephant
The following works wereusedin correlat- The Meseta Blanca Sandstone (Wood and
LITHOLOGY
l-l
Sondv
recl beds
n
Morine
m
Gypsum
m
EXPLANATION
Outcroosof Yeso Formotion
,t Sh.orplydefined boundory
( d o s h e dw h e r e
/
/
opproximote)
I
n
t e r ifn g e r i n g f o c i e s
-5r
trDoundory
- c o n t r o ll o c o t i o n
Outcroo
O
- 5-
corbonotes
Precombrion
rocks of
P e d e r n oul p l i f t
=v,/
Albuq
35"
OL\
]5u
Moriorty
Estoncio
o
o- Tl
<e^f,'
Vouohn
a
Laminae in the Caflas have thicknesses of
approximately l-5 mm, and the entire evaporite deposit is about 50 m thick. On the assumption of yearly cyclic deposition, this
thickness suggeststhat the evaporites were deposited over a period of 10,000-50,000yrs.
Jovrre S,qNosroNn MrNasrn-The Joyita
Sandstone Member was named by Needham
and Bates (1943). This coastal and eolian(?)
deposit consists of medium-bedded, tan to
red, fine- to medium-grained sandstone with
local interbeds of carbonate. It interfingers
with the continental red beds of the San
Ysidro Member of the Yeso north of Albuquerque and grades into carbonates near the
Sacramento Mountains (fig. l). The areal extent and geometry of this member closely parallel those of the underlying Caflas, suggesting
that the Joyita is a progradational beach and
dune facies associatedwith the withdrawal of
the Caflas sea.
Petrology
I
I
Tr uth
or
Thin sections of evaporite, clastic, and carbonate rocks from all members of the Yeso
Formation were prepared and examined according to methods summarized by Hunter
(1980). Twelve clastic samples were pointcounted to determine composition and provenance.
SaNpsroNn-Point-counting
results are
summarized in table l, and constituent ratios
are illustrated in fig. 3. Techniques employed
are those of Dickinson (1970), Ingersoll
(1978), and Ingersoll and Suczek (1979). The
95-percent confidence intervals for QFL and
LmLsLv (figs. 3a and 3b) overlap for the total
Yeso Formation and for each of its members.
o
q
c)
/
New AAexnc@
GEOLOGV
33'
. Scionce
andSetvice
Volume3,
oL
N
ie-|"
published
quarterly
by
New Mexico Bureau of Mines and Mineral Resources
a division of New Mexico Insritutc of Mining & Technology
i05*
FIGURE I -GpNrnal EXTENTANDFAcTES
BouNDARTEs
or Cnfias Cypsupt MEvnrn aNo coRRELATTvE
uNrrs;
INDICATED
LITHoLoctEswEREpREDoMTNANT
DUnrNcCnfrls oeposrrroN. The Pedernal uplift formed a ridge
along the east side of the Caflas Basin as far south as Pajarito Mountain (Kelley, 1968, 1971); by Cafras
time, the ridge was being covered by marine environments. Yeso sandstonesnear the Pedernal uplift are
arkosic due to their derivation from Precambrian basement (Kelley, 1968, l97l). Outcrop control at
numbered locations based on the following references: l) Hunter (1980), 2) Kelley and Wood (1946), 3)
L l o y d ( 1 9 4 9 ) , 4 )N e e d h a ma n d B a t e s( 1 9 4 3 ) ,a n d 5 ) K o t t l o w s k i ( 1 9 7 5 ) .
boundariesof the Cafras.The westernedgeis
typicallysharpand well definedand is characterizedby gypsumgradinginto sandstone
with
carbonateinterbedsover a distanceof from
lessthan 100m to I km. This edgeis exposed
in the centralFra CristobalRange,wherethe
presenceof brachiopodsand fusulinidsconfirms marine conditions (S. Thompson III,
personal communication, l98l). Near SoNovenber l98l
New Mexico Geologl
No.4, Novsmbor 1981
corro, the exactedgeof the Caflasis covered,
but no Caflas gypsum occurs in the Joyita
Hills, l0 km northwestof the Mesadel Yeso
type section(fig. l). The westernedgeof the
Cafiasis obscuredin manyplacesby structures
and strata of the Rio Granderift (Neogene).
To the east and southeast,the Cafiasgrades
into marine carbonatesthat are mapped as
yeso(undivided)by Baars(1962').
BOARD OF REGENTS
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LITHOLOGY
crossbedded
F-lll'l
I sondsrone
t
ITI-II.-l Mossive
l,:r,..i,,1,] sondslone
l=rjr-= j.l
li:,--:.1:H
beooeo slf slone.
shole. or
tr=;::.J-.,-l sondstone
l===-j
or shore
Limestone
ffi
%
o,"u^
common and may result from local segregacoarsenalong its flanks (Kelley, 1968,l97l).
By Caflastime, the subsidingland massprob- tion and concentrationof dark, organic-rich
ably forrned a submarineridge, thus restrict- carbonatematerial of the laminaeduring reing circulationand promotingevaporitedepo- peatedepisodesof recrystallization(Anderson
and Kirkland, 1960).Microfolds result from
sitionin theCaflaslagoon.
both externally induced deformation and diaThe high percentage(79 + 8 percent) of
metamorphiclithic fragments(fig. 4 and table geneticeffects.
Althoughgypsumis the only evaporitemin1) within total unstablelithic fragmentsin all
Yeso sandstones
examinedis consistentwith eral observedin outcrop, anhydriteoccursat
the interpretationthat the Pedernaluplift was depthsof lessthan 300 m. Drillers' logs from
a major supplier of clastic material for the an oil test in the Jornadadel Muerto near Enof halite in the upper
Caflas Basin. Most sedimentary lithic frag- gle indicatethe presence
mentsarelikely intrabasinalin origin (Hunter, Yeso(TennecoOil Company,unpublishedre1980).Volcanic lithic fragmentsare statisti- ports).
callynegligible(fie. 3b).
Depositionalmodels
All Yeso sandstonesexaminedin this study
The CaflasGypsum Member probably was
exhibit a similar diagenetichistory. An initial
in a barredmarine basinor lagoon,
deposited
by
quartz
was
followed
stageof
overgrowth
the developmentof authigenicclay coatings underconditionssimilar to thosedescribedby
(fig. a). This was followedby compactionand Schmalz(1969)for a salina-typemodel (fig.
pressolutionof quartz grains with attendant 5). Carbonateinterbedsin the evaporitesmay
squashingof monocrystallinephyllosilicate representbrief periodsof more normal salingrains and some conversion of softer lithic ity as a result of increasedseawaterinflux.
fragments into pseudomatrix (Dickinson, Clasticinterbedsmay be relatedto periodsof
1970).Compactionfeaturesare overlainby a progradationaldeposition of shorelineand
deposits.
secondstageof clay and/or other phyllosili- eolianfaciesand/or storm-related
Cyclic sedimentationcharacterizesthe Percate coatings.The final diageneticeffect was
the precipitationof sparrycalciteand the for- mian Systemin the study area. Thesecycles
mationof calciteveinlets.As a resultof calcite are relatedto changesin sealevel,the balance
and depositionrates,and
precipitation,little or none of the original betweensubsidence
the nature and amount of sedimentavailable.
porosityis preserved
in outcrop.
Gvpsuv-The gypsumfound in surfaceex- Cyclesare visible on a wide rangeof scales.
posuresof the Caflastypicallyis recrystallized Laminaeare cyclic on a scaleof millimeters;
as a resultof ground-waterinfiltration and at setsof sandstone,carbonate,and shalebeds
least one cycle of gypsum/anhydrite inver- are cyclic on a scale of meters to tens of
sion. A secondary"chicken-wire" textureis
ill
il,il,.
il:',",.,.
;
P
e
HO06
PA6-6-Pyl
HO07,HOO8,
HOrO,HOt2
HOO5
TABLE I -Pernocxlpruc coMpostrtoNsoF YesoseuosroNEs;original data from Hunter (1980);techniques
and terminologyfrom Dickinson(1970),Hunter(1980),Ingersoll(1978),and Ingersolland Suczek(1979).
PA6-6-Pym
a
6
c
^.9
nE
<E
tP
FICURE 2-Covposrrn srRATrcRApHrccoLUMNoF
rsn Yrso FonverroN (see Hunter [1980], for
descriptionsand locations of samples [numbers]).
thus supportingthe hypothesisthat all Yeso
in the study area share a similar
sandstones
provenanceand,/orare of equalmaturity.
The Pedernaluplift (fie. 1) appearsto have
beenboth the structuralcontrol and the source
of clasticmaterialfor the northernand eastern
margins of the Caflas Basin. This persistent
structuralhigh is composedof Precarnbrian
metamorphicrocks and was a local sourceof
clasticmaterialduring most of the Paleozoic
(Hock, 1970).This land masswas a positive
feature during Permiantime before Caflasdeposition,and Permiandepositspinch out and
Percent or
fraction
Component
Polycrystalline quartz
Monocrystalline quartz
Total quartz
Plagioclase feldspar
Potassium feldspar
Total feldspar
Metamorphic lithics
Sedimentary lithics
Volcanic lithics
Total unstable
aphanitic lithics
Monocrystalline
phyllosilicates
Miscellaneous framework
Total interstitial
(matrix, cement, voids, and
secondary minerals)
(Qp)
(Qm)
(Q)
(P)
(K)
(F)
(Lm)
(Ls)
(Lv)
2.8
44.2
(47.0)
5.1
10.0
(15.7)
8.3
2.4
0.1
(L)
(r0.8)
(M)
(MS)
(r)
1.4
1.2
2t.9
I 00.090
QFL% Q
QFL9o F
QFL9o L
64
2t7
15
10090
LmLvLs9o Lm
LmLvLs9o Lv
LmLvLs9o Ls
79
23
19
10090
Qp/Q
P/F
0.06
0.37
New Mexico Geology
Standard
deviation
Number of
samples
1.3
6.l
6.3
1.9
3.l
5.1
5.2
2.7
o.2
l2
12
t2
6
6
t2
12
12
12
't.t
t2
0.9
0.8
t2
t2
4.5
t2
'l
t2
ta
t2
l0
12
13
12
6
0.03
0.16
November l98l
o
too
(o)
Lm
(b)
too
All Yeso (Py)
(Grond ludn)
Joyrio Member (Pyl)
Coios M€mb6r (pyc)
Los Vollos Mgmbor (Pyl)
\)
plors sHowrNc
FIGURE 3-TntelculeR
a]uo sTANDARDDEvrArroNs (95-erncnNr coNFTDENcErNrEnvals) ron Ynso seNnsroNEs. Seetable"ro"
I for summary data and symbols; a) QFL triangle, b) LmLsLv
triangle.
itation of marinesalts.This basinis locatedin
a temperatedesertregionand is surroundedby
sandyshorelineand dunedeposits.
In addition to being similar to the Caflas
Basin in size, physiography,climate, and
depositional environment, the Kara-BogazGol has a similar tectonicsetting.The KaraBogaz-Goland CaspianSeaare, in part, remnants of the once more extensiveTethys Sea
that has closed during complex continental
collisionsin the Mesozoicand Cenozoic(Sengor, 1979). In an analogoussituation, the
CaflasBasinor lagoonwasa small part of the
Permianbasinsof southernand easternNew
Mexicoand westTexas,all of whichrepresent
the last vestigesof a oncemore extensiveremnant oceanbasinthat was closedduring continental collision in the late Paleozoic
(Ouachita-Marathonorogeny)(Graham and
others,1975).The Pedernaluplift and related
deformationmay be responsesto this continental collision(Coney, 1978;Kluth and Coney, l98l; Woodwardand Ingersoll,1979).
Frconomics
The CaflasGypsum Member extendsover
an areaof approximately25,000km' (fig. l).
an averagegypsum/anhydrite
FIGURE 4-Typrcll
Cnfies GypsuNaMENrsEn If one assumes
sANDsroNE
wrrH MoNocRysrAlr_rNr
quenrz (eu),
thicknessof 30 m, this indicatesa total sulMETAMoReHTC
LlrHtc FRAcMENT (Lu), pI-Aclo.
phate tonnage of about 1.5 x l0r': metric
CLASEFELDSnAn(P), nNo cALcrrE (C) (sEcoN- tons. Gypsumis an important industrialminoenv?). Note concavoconvex grain contacts,
eral; New Mexico produced4.1 x 105metric
suturing of grains, pressolution, overgrowth on
tons with a valueof $4.3 x 106for the years
grains,
phyllosilicate
and
coatings; crossed
Qm
1977-1978(Eveleth and Kottlowski, 1980).
nicols.
The United Statesconsumed3.7 x l0? metric
meters;lithologiesof Yesomembersarecyclic
on a scaleof tensto hundredsof meters:and
the entire Permian Systemin the study area
may representa seriesof transgressions
and
regressions
that depositedhundredsof meters
of interbeddedmarine and continentaldeposits.
A similar modernenvironmentis the KaraBogaz-Gol,a hypersalinebay (approximate
area18,000km'?and depthabout l0 m) linked FICURE 5-Srrr.rplrrrro sALTNA-TypEMoDEL oF AN
EvApoRrrE uesrN (modified after Briggs and Polto the CaspianSeaby a narrow strait. This
lack, 1967) showing: surface-water isosalinity
region has been studied and describedby
lines (90), direction of near-surface currents (arDzens-Litovskiy(1967) and Dzens-Litovskiy
rows), and area of mesosalineenvironment (crossand Vasil'yev(1962),who reportactivepreciphatched). (Kirkland and Evans, I981.)
52
November1981
New Mexico Geology
tons($2.4 x 108)in the sameperiod,of which
approximately3l percentwasimported(Pressler, 1979).The Caflasrepresentsa significant
gypsum resource,and further exploration of
near-surface
depositsis indicated.
Conclusions
The CaflasGypsum Member was deposited
during a 10,000-50,000-yr
interval of relative
sea-levelstabilityin a marinelagoonor basin
connectedacrossshallowshelvesto the deeper
Permianbasinsto the south and east.The location, geometry,and facies boundariesof
this basin were controlled, in part, by the
Pedernaluplift, which also was a sourceof
clasticmaterial.The restrictedbasinalconditions of all Permian basins of southeastern
New Mexico and west Texasowe their origin
to the Ouachita-Marathonorogenycausedby
continentalcollision.The sizeand thicknessof
the Cafiasevaporitesmake thesedepositsan
importantmineralresourcefor New Mexico.
AcrNowreocMENTS-The authors thank
TennecoOil Company,MineralsExploration,
for funding a SeniorHonors Thesis(Hunter,
1980)on which much of this paper is based.
Appreciationalso is extendedto J. L. Wilson
and D. L. Emmons(Tennecogeologists)for
their assistance
and comments.J. F. Callender, V. C. Kelley, F. E. Kottlowski, and S.
ThompsonIII alsoreviewedthis paperandare
gratefullyacknowledged.
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!
57
in
stratapenetrated
EarlyTertiary(?)
delMuerto
Jornada
rs,
b yG .E .S c h w aRb.,M .C o l p i tJt sr ., ,a n dW .
NM
Inc, Socorro,
& Associates,
W.KSummers
with othersworking in
Rocks that appearto be of early Tertiary additionto discussions
by four wellsdrilledin the the area, indicate that all four wells may
agewerepenetrated
Jornadadel Muerto nearEngle,New Mexico, penetratedifferentatypicalphasesof the Palm
Park Formation(Eocene).
during 1979and 1980.
Thesecorrelationsare uncertainand more
Samplesfrom SERA #l and TAC #2 wells
havebeenfiled with the New Mexico Bureau detailedstudy could show that all or part of
in Socorro, the strata belong in the Thurman, Love
of Mines and Mineral Resources
New Mexico,wherethey may be examinedby Ranch, or McRae Formationsinsteadof the
Palm Park Formation. Of theseformations,
interestedparties.
No other wells in this part of the Jornada only the McRaeFormationhasbeenidentified
del Muerto penetraterocks of similar charac- this far north in the Jornadadel Muerto. It octer or apparent age. All four wells penetrate curs as isolatedoutcropsnear the railroad in
outcrops
strata that apparently representpost-Mesa- T. l2 S., R. 2 W. as wellas extensive
along the eastshoreof ElephantButte Reserverdebut pre-SantaFe deposition.
l) TAC #2well is located783,100ft north, voir: Sun-Victorio#2 well in sec.27, T. l0 S.,
746,500ft east(New Mexico coordinate R. I W. penetrated39 ft of McRae(?)Formasystem,west zone);total depthis 500ft; tion. Frank Kottlowski(personalcommunica60 ft are sedimentsand sedimentary tion, l98l) recallscuttingsof McRaeFormarocks (presumably of the Santa Fe tion from a seriesof seismicshot holesalong
Group); lower 440 ft are grayish-red, old NM-52 eastof Engle.
Whateverthe ultimatecorrelation,the rocks
brownish-gray,and grayish-brownrhyoinvolvedare atypicalof the earlyTertiary forlite and latitic tuffs and breccias.
!
in the basin.
2) JDC #l well is located797,100ft north, mationselsewhere
744,900ft east(New Mexico coordinate
system,west zone);total depthis 500ft,
mostly in gray, red, and blue sedimentary rocks (someprobably volcaniclastic); onevery hard red "sandstone"may
be a volcanicflow.
3) JDC #2 well is located800,250ft north,
745,000ft east(New Mexico coordinate
system,westzone);total depthis 300ft,
mostly in gray, red, and blue sedimentary rocks;lowest75 ft areprobablyvolcaniclasticor volcanic;lowermost33 ft
areprobablyrhyolite.
4) SERA #l well is located 830,700 ft
north, 737,600ft east(New Mexico coordinatesystem,west zone);total depth
is 345 ft, in sedimentsand sedimentary
oTAc # 2
rocks;belowuppermostI 14 ft (SantaFe
Group), well penetratedred, brown,
is_ _.-gray, and, occasionally,purple sedimentsand sedimentaryrocks; few samplesmay includevolcaniclastics.
Rrw
R4w
R3w.
i
i
Our cursory examinationof the drill cut'l
tingsfrom SERA #l andTAC #2 wellsand the
or2545rom
drillers' logs of JDC #l and JDC #2 wells,in
iq
ii
New Mexico Ceology
November l98l