Qec
from 10–200 cm in height. Sand is very fine- to medium-grained (mostly fine-grained), with 1–5% coarse to very coarse, scattered sand grains.
Coppice dunes overlie a bioturbated eolian sand sheet or sheetflood deposits (with a sparse pebble lag). Loose. Deposit under the dunes is up
to ~2 m thick. Unit includes coppice dunes developed on sand ramps, where the entire eolian deposit may be several meters thick.
Eolian sand in dune forms other than coppice dunes (middle to upper Holocene)—Eolian sand in mound-like deposits that extend over several
meters. Dunes are 30–100 cm tall, commonly elongated NE–SW (3–30 m in length), and overlie sheetflood deposits or eolian sand sheets correlNMBGMR
Open File Report
ative to Qse (included with this unit). Sand is light brown to reddish-yellow and fine- to medium-grained. Loose
and up to 3 m thick.
Qed
NEW MEXICO BUREAU OF GEOLOGY & MINERAL RESOURCES
563
Last Modified 30 June 2014
NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY
A DIVISION OF
Sheetflood and slopewash deposits, commonly reworking eolian sand sheets (middle to upper Holocene)—Light brown to brown to reddish
yellow, very fine- to medium-grained sand (minor coarser-grained sand). May be composed of pale brown, clayey–silty, very fine- to fine-grained
sand at the base of steep slopes. Both deposits contain minor (1–5%), scattered, very fine to coarse pebbles. A very thin pebble bed may be
present at base of deposit. Internally massive with weak cumulic soil development characterized by ped development and minor gypsum accumulation. Local, very thin to thin sandy pebble lenses. Unit locally grades laterally into Qay. Surface commonly has a sparse lag gravel and no to
weak desert pavement development. Loose to moderately consolidated. 0.2–3 m thick.
Qse
33
Kg
Kg
Qls
Qao2
8
12
88
76
5
22
Qao2
Kc
Qls
Tist
Qay
64
S1 inclined foliation
50
S2 inclined foliation
Qay
Qao2
Qao2
Qse
Kg
Qse
Kg
9
Qse
Psr
12
Qct Psr Qct
Qse
7
Qse
53 Py
24
Psr
Py
Psr
Py
12
Qse Psr
Qao
Qao2
5
Psr Py
Psr
Qse
Qao
Py
Psr
13
Qar
Qar
14
Qar
Qar
Py
Qse
Qao1
5
Pag
Pag
Pag
Qao1
Qse
Tist
69
Qbm
Qay
Qse
Qse
Qse
Qay
Qao Qao
Qao1
Qayr
Qayr
Qao2
Qao2
Qayr
Qao1
Qao2
Qao
Qay
Qao Qao Qao2Qay Qay
Qao2
Qao
Qao Qao
Qay
Qayr
Qayr
Qay
QayQao1
Qao1
Qao1
Qay
Kc Qayr
QayrQayr
Qayr
Qao1
Kc
Kc
Qao1
Kc Qao1
Qayr
Qayr
Qay
Qao2
Qao2
Qao2
Qao2
Qao
Qao3
Qao2
Qao
Qao2
Qao3
Qao2
Qao
30
Kc
Qao
Qao2
Qao
Qao2
Qay
Timd
Qao
Qao
Qao
Qar Qao
af
35
Qay
Twh
Qao3
Twh
Qao2
Twh
17 Ts
Qay
Qao2
24
29
Qao Qay
15 24Qao
Tirg
12
Qao
Qao
Qay
20
15
15 Kc
Qao2
Qao3
Twh
Qay
Qay
Qay
Qay
Qao2
Qao3
Qay
QarQay
Qay
Qay
Qao2
Qay
Qao2
Qayr
Qdsct
Qao
Qao Qao
Qao2
Qao
Qao
Qao3
Qay
Kc
16
16
Qao1
25
Kg
Qao Qao
Qao Qay
Qao
Qao Qdsct
Qdsct
Qdsct
Qao
Qdsct
Kc
Qay
29 18
Qao
Qar
Qay Kc
Qao
17
Kc
Qao
Qdsct
Tirg
Qar
Qao3
Qayr
Qay
Qay
Qar
Qay
Qao2
Qay
Qay
Qao2
Qao2
Qay
Qayr
Qao3
Qao1
Qao3
Qao3
Qay
Qao2
Qao
Qao
Qao2
Qar
Qay
Qao1
Qary
Qao
Ts
Tid
Qay
Ts
Ts
Timd
Timd
30
29
28 Ts
Qao Ts
Qao
27
Qar
Ts
Qay
Twh
Qay
Qao
Qse
Twh
Qse
Twh
Qao
Twh
Kc
Qao
40
Tirg 34
Tirg
10
Qay
Qao1
Qct
Qao
45
50
break
80
Tstg
Tsrqd
Tgjta
Tsts
The youngest allostratigraphic
unit back-fills narrow paleovalleys cut in the second-oldest unit, and consists of pale brown to very pale brown to
Tgjbt
Tirt
light brownish-gray,
sand with minor beds of pebbles. The top soil of the youngest allostratigraphic unit is marked by slight calcium
Tgjb, well-stratified
Tigjb
TirgAge control from Koning, 2009). 1–4 m thick.
and gypsum accumulation
(comparable
to a Stage I calcium
morphology).
Tgjpt
Tsb carbonate
Tsx
Tist
qv
Tgjt
Tgl
Younger
alluvium,
with
subordinate
recent
alluvium
(Holocene)—See
descriptions
for
units
Qay
and
Qar.
Mapped
near
modern
drainages
Qayr
Tnpt
where Qay and Qar could not be differentiated at this map scale.
Ti
Titb Tita Timd Titd Timp
Twbpt
Younger alluviumTwtd
overlying intermediate alluvium—Generally mapped in the west–eastTid
valley north of the Godfrey Hills. See descriptions for
Qay/Qai
Tim
Twtatunits Qay and Qai.Twtt and Tws Twt
Tcp, Tkgf
Twtr
Twh (uppermost Pleistocene)—Unit locally seen in arroyo cuts disconformably between units Qao below and Qay1 above.
Intermediate alluvium
Ts Sediment consists of reddish-brown, commonly clay-rich, very fine- to very coarse-grained sand and pebbly sand that is massive; pebbles occur
95
100
Tc
?
230
Qao
?
26
260
270
locally occupying paleo-valleys. Contains interfingering coarse channel-fills and finer-grained deposits that locally exhibit a coarsening-upward
trend. Gravel is clast-supported, locally imbricated, gypsiferous (but seemingly less gypsum than in units Qao2 and Qao1), and consists of very
fine to very coarse pebbles with subordinate to subequal cobbles and 1–25% boulders. Debris flow sediment is locally observed (<10% of
Kclt sediment volume away from bedrock highs) and commonly has matrix-supported cobbles. Sand is mostly medium- to very coarse-grained. Coarse
Kg beds are weakly to moderately consolidated and non-cemented. Thick clay colloids commonly coat sand grains and clasts.
Kmd
Finer-grained sediment is light brown (7.5 YR 6/4) to reddish-yellow (7.5 YR 6/6) to reddish-brown (5 YR 5/4), hard, gypsiferous, and composed
Kt of silty-clayey very-fine to fine-grained sand (locally with medium to very coarse sand) in thin to thick, tabular beds (also internally massive). Within
Kmlthe floodplain sediment are 20–25% interbeds of fine- to very coarse-grained sand and sandy pebbles; these coarse beds are very thin to thin and
lenticular to tabular. There may also be up to 5–15% scattered pebbles and up to 15% scattered medium- to very coarse-grained volcanic sand.
The tread of this unit lies as much as 6 m below adjacent Qao2 surfaces.
Kd
On the surface, clast varnishing is relatively strong, and there is a well-developed desert pavement where unit is not covered by slopewash or sheet-
? ?flood deposits (Qse). A strong gypsum horizon (comparable to a Stage III calcium carbonate morphology) is developed on top of this unit to the
Middle allostratigraphic subunit of older alluvium (middle to upper Pleistocene)—The extensive Qao2 probably represents multiple aggradational events that were amalgamated into seemingly one deposit. Unit consists of interbedded fine-grained sediment and sandy gravel and pebbly
sand, and locally exhibits a coarsening-upward trend (where the upper part consists of amalgamated or stacked channel-fills). Finer sediment
consists of gypsiferous, reddish to very pale brown, very fine- to medium sand and clayey fine sand, with minor coarse- to very coarse-grained sand
TRm,
and pebbles (scattered or in very thin to medium lenses). Buried soils commonly have a relatively thin, slightly reddened horizon (locally with illuviatTRed clay) underlain by a calcic horizon (Stage I to II carbonate morphology) underlain by a gypsic horizon. Locally, rhizoliths are present that are
cemented by gypsum.
Base of unit lies several meters below the base of unit Qao1, and its surface contains strong gypsum or calcic/gypsic horizon(s) with Stage III-IV
apparent carbonate morphology. Strong clast varnish and a well-developed desert pavement where unit is not covered by slopewash or sheetflood deposits (Qse). Several non-differentiated erosion surfaces. Weakly to well consolidated, non-cemented. Unit grades downward into Santa
PagFe Group deposits west of the Alamogordo fault. Exposures are 3–15 m thick.
Psf
Older allostratigraphic
subunit
older alluvium (lower to middle Pleistocene)—Sandy gravel under topographic highs, locally overlying
Pg in subsurface
near of
Carrizozo
Psh
bedrock, that grades westward into intercalated sandy pebbles, pebbly sand, sand, and clayey-silty sand. Finer-grained sediment
Psr exposed
appears to dominate progressively south of the Three Rivers drainage. Unit lacks the buried soils that are commonly observed in Qao2, typically
Pycontains coarser gravels, and is locally very gypsiferous. The unit contains a basal sandy gravel, 1–3 m thick and commonly strongly cemented,
which is overlain by a coarsening-upward sequence. Sandy gravel is dominated by stream-flow facies, with lesser amounts of debris-flow facies.
Gravel is mostly clast-supported, locally imbricated, and consists of pebbles with subequal to subordinate cobbles and boulders. About 1–3% of
clasts disintegrate readily. Sand is mostly medium- to very coarse-grained. Debris flow sediment contains abundant cobbles and boulders that are
commonly matrix-supported. Fine-grained sediment ranges from reddish to very pale brown. Clay, silt, and very fine- to fine-grained sand become
increasingly common away from the mountain front. Sand in fine-grained deposits is mostly very fine- to fine-grained, with subordinate medium to
very coarse grains that are commonly scattered. Base of deposit is typically >6 meters above the base of unit Qao2. In the south, a prevalent petrogypsic horizon developed on its surface with very strongly varnished surface clasts. In the north, top soil is characterized by strong calcium carbonate + gypsum accumulations (Stage III to IV calcium carbonate morphology). Weakly to moderately consolidated. 1–35 m thick.
Qao1
TRIASSIC
QTg
Tbf
Qbm
Ti
Tirg
Tigjb
Timd
Tirt
Tid
Tist
Titd
Timp
Tita
Titb
Tim
Tsb
Tstg
Tsts
Tstag
9000
8000
6000
Qbm overlying Qa
TR
Qa
Kd
Pag
Pg
4000
Qa
Qbm
5000
TB-204
7000
3000
Kg
Kmt
Kml
Kmd
Kd
TR
Pag
Ps
Pag
Ps
Pg
Thicknesses of Triassic and Permian strata are from the Ralph Federal well (Broadhead and Jones, 2004)
0
20000
10000
40000
Qa
5000
Kd
TR
4000
Py
3000
TR
Ps
Pg
Km
Pag
Kml
1000
0
20000
10000
Kt
Kd
TR
Pag
Pg
Py
Kg
Kmd
Kml
Pag
Pg
Ps
8000
TB-237
TB-238
TB-40
9000
7000
Nogal fault
Kc
Kd
Kclt
Kg
Kmd
Kml
TR
Ps
Pag
60000
50000
6000
Kt
Kmd
Kml
TR
Pag
4000
3000
Ps (Pg too thin to differentiate and subsumed into Ps)
Kt
Kml
Kd
TR
0
80000
Qa
Qbm
Kt
5000
TR
4000
3000
Py
2000
TB-185
TB-184
Twtat
Kclt
Kd
Py
Twh
Kth
20000
Ts
Pag
Pg
Ps
Kclt
Kd
Kt
Kd Kml
Py
30000
40000
50000
Kcl
Kclt
Kg
Kcl
60000
Cross-section F-F’
Church Mtn quad
Nogal Pk quad
7000
Twh
6000
5000
Kcl
Kmd
Kcl
Kclt
Kt
Kml
Trm
70000
Tc
4000
Kcu
3000
Kcu
Tsrs
Timd
Kg
Kmd
Kml
Kd
Qao1
1000
Kt
0
90000
Kcu
Tc
Kclt
Kg
Kmd
Kt
Kd
Kcl
Km
l
Tr
Pagm
Ps
Kd
Alamogordo
fault zone
Psr
Qa
6000
Qbm
5000
QTbf
4000
Py Py
1000
Pa
Kd
Py
Pa
Py
Pa
20000
Psf
Psr
40000
Kg
Kt
Kd
Trm
Kmd
Kml
Kclt
Kd
Psf
Kt
Trm
Psr
Tita
Tist
Pa
Kcu l
Kc
clt Kg
K
Kcl
Kg
Kmd
Pag
Kd
Kt
Kd
Kt
Kml
Trm
Pag
Psf
Psr
Psf
Py
Kclt
Kcc
Kcc
Kml
Tita
Kd
Kd
Kml
Kd
TRm
TRm
Kmd
Kth
Kml
Kd
Kth
Kd
TRm
Pag
Pag
80000 ft
Kg
Psf
Kmd
Psr
Kml
Py
TRm
Pag
Kg
Kg
Kmd
Kth
Kth
Kd
Kd
Kg
Kml
Kmd
TRm
Kg
Kml
Kd
TRm
Psr
Kth
TRm
Kd
Kml
Kth
Cross-section I-I’’’’
Kd
Psf
Pag
Psf
Py
Kg
Kt
Kd
Trm
Pag
Psf
Psr
Kg
Kmd
Kml
d
Km
l
m
K
Trm
Pag
Psr
Kmd
Pa
Kcu
Kt
Kml
Psr
Py
100000
80000
Kcl
Pag
Kd
Trm
Ts
Tc
Kcl
Kmd
Psf
Tc
Kcl
Kml Kt
Kg
Pag
Kt
Kml
160000
Kclt
Kmu
Twhf
Kg
Kt Km
u
Kml
Kcl
Kclt
Kg
Kth
Kmd
Kth
Kml
Kd
TRm
Kmd
Kml
Kd
TRm
Pag
Kth Kml
Kd
TRm
Pag
Psf
Kmd
Kml
Kd
TRm
Pag
Psf
Psr
Psf
Kml
Kd
TRm
Pag
Twtd
Twtat
Tws
Twtt
Twhs
Ts
120,000 ft
Kclt
Kg
Kt
Kml
Kcl
Kmd
200000
Kml
Kd
TRm
Pag
Psf
Psr
Psf
6000
Kth
Kmd
Kml
Kd
TRm
Pag
Kml
Kd
TRm
Pag
Psf
Psf
Psr
Psr
Py
Py
Tita
Kml
Kd
TRm
Pag
5000
Psr
Py
Py
Py
2000
Py
Psf
Kclt
Kg
Kmd
Kml
Twtr
Psr
Pa
Pa
Pa
Pa
Pa
Pa
1000
Pa
Pa
130,000 ft
Pb Pb
Pb
Pb
0
Pb
Twh
Pb
140,000 ft
Kmd Kt
5000
Psf
Kml
Trm
Pag
Psf
Py
4000
Psr
3000
Kml
Kd
Kml
Kd
Trmg
Pa
Psf
2000
Kd Trm
Trm
Trm
Pag
Pag
Pag
Psf
Psf Psr
Psr
Py
Psr
Py
Py
Py Py
Pa
1000
Kml
Pa
Pa
Kd
Qa
Trm
Pag
Psr
Kml
Kml
Qa
Trm
Pag
Psf
Kt
Kml
Trm
Psf
Py
Kc
Kg
0
Pa
Pa
Pa
Timd
Twhs
E’’’’
Ts
8000
Rhyolite to trachyte (Oligocene)—White to gray,Nogal
aphyric
fault to porphyritic, felsic intrusions interpreted to be of rhyolite or trachyte composition.
7000
Qa
Twtr consist of dikes and
Qa
Twh
Intrusions
small
plugs
associated
with
the ThreeTcRivers stock. Phenocrysts include Kspar, quartz, biotite, and plagioclase.
Qa
Ts
Twtr
Kcu
Locally,
rhyolite are included
inTcthis unit; these are6000
typically flow-banded and folded and contain microphenocrysts of
Twh flows of aphyric
Twh
Ts
Kclt Kcl of Goff et al., 2011). Unit also includes fine- to coarse-grained, pale pink to pale
quartz). are included in this unit (i.e., Oak Grove rhyolite
5000
Ts
Kgminor biotite, and arfvedsonite (these cut the Walker Group and various syenite units).
tan dikes containingTsKspar, quartz, minor Tc
plagioclase,
Kcu
Tc
240000 Society Guidebook 42, p. 97–113.
220000
regional
and
deposits:
New
Geological
to tectonics
gray. Stocks
andmineral
many other
intrusions
areMexico
commonly
porphyritic,
with phenocrysts composed of orthoclase and plagioclase that are 1–20 mm
Tc
for
Ts
Py
Psr Psf
20000
10000
Kcu
Kmd
Kt
Kd
Kml
T
Pag rm
40000
Kg
Kcu
Kcl
Kclt
Kd
Kcl
Kg
60000
Kcu
Tita
Kcl
Kclt
80000
Kg
Kcl
Kg
Tc
Psf
Kt
Kml
Trm
Pag
TB-192
TB-193 & 194
Tc
Twh
Ts
Tc
Tc
Kt
Kd
Kml
Trm
Pag
Psf Psf
Kmd
Py
100000
Kcl
Kg
Kmd
Kmd
Trm
Kt
Kml
Trm
about 15–20% large phenocrysts
(0.1–2.0 cm long) of tabular plagioclase in an equigranular to fine-grained matrix of plagioclase and pyroxene
9000
(0.1–0.5,
The plagioclase
laths are
oftenfrom
distinctively
the margins
of the dikes.
Probable ME.,
intrusive
equivalent
Cobban,
W.A.,mostly
1986,0.1–0.3
Uppermm).
Cretaceous
molluscan
record
Lincolnaligned
County,parallel
New toMexico,
in Ahlen,
J.L., Hanson,
and
Zidek, J., eds.,
8000
of megacrystic plagioclase-bearing
lavas in the Rattlesnake Member of the Three Rivers Formation, which is the basis of the upper Eocene age
Southwest
Section of AAPG Transactions and Guidebook of 1986 Convention, Ruidoso, New Mexico: New Mexico Bureau of Mines and MinerTwt
interpretation.
7000
al
Resources,
p. 77–89.
Twh
Kd
160000
including minor trachybasalt (upper Eocene)—Porphyritic intrusive rocks that are common throughout the map area,
6000
Tita Trachyandesite intrusions,
Compton,
R.R., 1985,
Geology
in or
thesills.
field:
New
York,
Wileylight
& Sons,
p. locally weathering to reddish-brown to brownish-gray.
commonly
occurring
as dikes
These
rocks
areJohn
typically
gray toInc.,
dark398
gray,
5000
Exposed rocks generally do not develop as strong a varnish as that on Tim. Up to 35% phenocrysts of pyroxene (0.5–10 mm-long) and feldspar
Dowe, (probably
C.E., McMillan,
N.J., McLemore,
Hutt, hornblende
a., 2002, Eocene
magmas
of the Sacramento
NMaligned.
– subduction
or rifting?:
plagioclase,
0.5–11
long);and
locally,
phenocrysts
are observed.
Feldspars Mountain,
are commonly
Groundmass
is New
4000 mm V.T.,
ranges from 0.1–0.5 mm together with 10–35% pyroxene(?) ± biotite (0.1–0.5 mm long).
Mexicocomposed
Geology,of v.feldspar
24, p. that
59–60.
Ts
Tsrs
Tc
3000
Kcu
Kcl
Kclt
Kg
Kmd
Kt
Kd
Kml
Trm
140000
120000
Kcl
Kclt
200000
Megacrystic, alkali gabbro–diorite or syenogabbro–diorite intrusions (middle? to upper Eocene)—Dark gray to gray to greenish-gray,
Tim
0
Gile,
L.H.,
Hawley,
J.W., androcks
Grossman,
R.B.,
and geomorphology
Basin mm,
and less
Range
area oftoSouthern
Mexicoof— Guide220000
porphyritic
hypabyssal
occupying
sills,1981,
dikes,Soils
and laccoliths.
Groundmassinis the
0.2–0.5
commonly
1.0 mm,New
and consists
book toplagioclase
the Desertwith
Project:
Newpyroxene
Mexico Bureau
of Mines
and Mineral
Resources,
Memoir 39,composed
222 p. of hornblende ± pyroxene (up to
15–25%
and local
hornblende.
Rock has
2–25% phenocrysts
20–60 mm long) and 5–20% smaller plagioclase. Groundmass consists of plagioclase with subordinate, but variable, amounts of mafic
Elevation
(ft)
Pa
g
Pa
Ps
1000
0
Py
Pa
Py
Pa
Pa
Ps
K
Km g
d
KmKt
l
r
40000
Kc
Kcl
t
Recharge zone
on Three Rivers
allvuial fan
6000
5000
Three Rivers
Railroad Well #2
(TB-056)
QTbf
4000
Tl
Tl
Tl
1000
Ts
Kc
0
Alamogordo
Kd
fault
Trm
Kc Pag
Kclt
QTbf
QTbf
3000
2000
Three Rivers
Railroad Well #1
(TB-057)
10000
Ts
Kc
Kg
Kmt
Kd
Trm
Pag
Ps
Pa
Py
Kd
Ps
Trm
Pag
Ps
Probable
perched,
unconfined
aquifer in Qa
Qa
Three Rivers N
Ranch house well
(TB-059 for
lithology & TB-060
for GW level)
Kd
Kml
Kc
Psr
TB-148
Psf
Tita
Ts
Twh
4800--ignored
Twh
Ts
Ts
5243 (projection using 25 degr att)
Ts
Tist
Tc
Tist
Kclt
Kmd
Kg
Tc
Ts thins to south
Ts
Psr
Kg
Kmd
Kclt
Py
Tig
Tita
Twh
Ts Tc
Ts
Tcm
Kclt
Kgs
Kml
Trm
Pag
Trm
Pag
Kd
EastThree
Rivers
Petroglyph
Tcm fault
Compton, R.R., 1985, Geology in the field: New York, John
Wiley & Sons, Inc., 398 p.
Qa
Three Rivers
fee well
(TB-244)
TB-63
Twh
Twh
Ts
Ts
Twt
Twt
Kc
Kclt
lt
Tc
ml
Kd
Trm
Pag
Kmd
Kg
Kclt
Kg
Kg
Kmd
Ps
Pag
Trm
Ps
Tc
Qa
Little Bear Canyon
Aspen Canyon
South Fork
Rio Bonito
Canyon
Big Bear Canyon
I’’’’
Twt
Tc
Tc
Tc
Tc
Kelley, V.C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and Mineral Resources, Memoir 24,
?
Kc
75
Kc p
Kc
Kc
Kclt
Kclt
Kclt
Kelley,
V.C., 1972, Geology of the Fort Sumner sheet,
New Mexico: New Mexico Bureau of Mines
and Mineral Resources, Bulletin 98, 55 p.
?
Kg
Kg
Kt
Kd
Trm
Pag
Kmd
Kml
Kg
Kmd
Kml
Kt
Kd
Trm
Koning, D.J.,80000
2009, Radiocarbon age control
Mountain-derived alluvial fan deposits near Alamogordo, New Mexico, and related
Pag for Sacramento
110000
90000
100000
geomorphic and sedimentologic interpretations [abstract for 2009 NMGS Spring Meeting]: New Mexico Geology, v. 31, no. 2, p. 46.
Gillette, D.D., Wolberg, D.L., and Hunt, A.P., 1986, Tyrannosaurus Rex from the McRae Formation (Lancian, Upper Cretaceous), Elephant Butte
Reservoir, Sierra County, New Mexico: New Mexico Geological Society, Guidebook 37, p. 235–238.
Kues, B.S., Lucas, S.G., Kietzke, K., and Mateer, N.J., 1985, Synopsis of Tucumcari Shale, Mesa Rica Sandstone, and Pajarito Shale paleontology,
Cretaceous of east–central New Mexico: New Mexico Geological Society Guidebook, 36th Annual Field Conference, p. 261–281
11000
Palisades Tuff, and trachyte breccia. 5–15 m thick. The lower unit is a sandy, matrix-supported, carbonate-cemented conglomerate that contains
39
10000
McManus,
N.J., 2002,
Subduction
or rifting:the
magmas
of the
thelower
Sacramento
Geological
Ar date
of 28.23 Society
upperC.E.D.,
trachyteand
lavaMcMillan,
as the dominate
clast. Locally
preserved
vitric, lithic Eocene
tuff interbedded
with
sedimentMountains,
has an 40Ar/NM:
of America
Abstracts
with
Programs, v. 34, no. 6, p. 364.9000
± 0.06
Ma. 30 m
thick.
Qls
Twt
Twt
Qayr
8000 Formation
trachyandesite
of Petroglyph
the Jackasssite,
Mountain
(lower
Oligocene)—Light
to dark graymini-paper]:
fine-grained New
lava with
a trachytic
Tgjta Trachyte
McLemore,
V.T.,to2002,
The Threeflows
Rivers
Otero
County, New
Mexico
[non peer-reviewed
Mexico
Geological
texture
and
contorted
platy
flow
foliation.
The
unit
is
composed
of a series of thin flows 1–10 m thick with basal scoriaceous breccia and vesicular
Tsx Conference
Tsb
Society, 53rd Twh
Annual Field
Guidebook, p. 26–27.
7000
Tsts
TwhV.C., and Tw
h
Kelley,
Thompson,
T.B., 1964, Tectonics
and general geology of the Ruidoso-Carrizozo region, central New Mexico: New Mexico
Ts
Ts
?
Ts
?
Ts
Geological Society,
15th Field Conference Guidebook, p. 110–121.
Tsts
6000
Ts E.E., Meyer, G.A., and Smith, G.W., 1988, Geologic map of the northwestern part of the Mescalero Apache Indian ReservaMoore,Biotite
S.L., Foord,
trachyte within trachyte to trachyandesite flows of the Jackass Mountain Formation (lower Oligocene)—Flow of trachydacite with
Tgjbt
tion, Otero
U.S. Geological
Survey
I-1895,
biotiteCounty,
setTcin a New
sugaryMexico:
matrix interbedded
with Tgjta.
At 5000
oneMap
locality
on thescale
east 1:24,000.
side of Jackass Mountain, this unit consists of altered tephra (< 1
Tgjpt
Soil Survey Staff, 1992, Keys to Soil Taxonomy: U.S. Department of Agriculture, SMSS Technical Monograph no. 19, 5th edition, 541 p.
Birkeland, P.W., Machette, M.N., and Haller, K.M., 1991, Soils as a tool for applied Quaternary geology: Utah Geological and Mineral Survey,
a division of the Utah Department of Natural Resources, Miscellaneous Publication 91–3, 63 p.
Hook, S.C., 2010, Flemingostrea elegans, n. sp.: guide fossil to marine, lower Coniacian (Upper Cretaceous) strata of central New Mexico: New
Mexico Geology, v. 32, no. 2, p. 35–57.
Lucas, S.G., 1991, Correlation of Triassic strata of the Colorado Plateau and southern High Plains, New Mexico: New Mexico Bureau of Mines
and Mineral Resources, Bulletin 137, p. 47–56.
Lucas, S.G., 2004, The Triassic and Jurassic systems in New Mexico, in Mack, G.H., and Giles, K.A., eds., The Geology of New Mexico, A Geologic History: New Mexico Geological Society, Special Publication 11, p. 137–152.
Cobban, W.A., 1986, Upper Cretaceous molluscan record from Lincoln County, New Mexico, in Ahlen, J.L., Hanson, ME., and Zidek, J., eds.,
Southwest Section of AAPG Transactions and Guidebook of 1986 Convention, Ruidoso, New Mexico: New Mexico Bureau of Mines and Mineral Resources, p. 77–89.
Hook, S.C., Molenaar, C.M., and Cobban, W.A., 1983, Stratigraphy and revision of nomenclature of upper Cenomanian to Turonian (Upper
Cretaceous) rocks of west–central New Mexico, in Hook, S.C. (compiler), Contributions to mid-Cretaceous paleontology and stratigraphy of New
Mexico – part II: New Mexico Bureau of Mines and Mineral Resources, Circular 185, p. 7–28.
Ingram, R.L., 1954, Terminology for the thickness of stratification and parting units in sedimentary rocks: Geological Society of America Bulletin, v.
65, p. 937-938, table 2.
Compton, R.R., 1985, Geology in the field: New York, John Wiley & Sons, Inc., 398 p.
Dowe, C.E., McMillan, N.J., McLemore, V.T., and Hutt, a., 2002, Eocene magmas of the Sacramento Mountain, NM – subduction or rifting?: New
Mexico Geology, v. 24, p. 59–60.
Gile, L.H., Peterson, F.F., and Grossman, R.B., 1966, Morphological and genetic sequences of carbonate accumulation in desert soils: Soil
Science, v. 101, p. 347–360.
Kelley, V.C., and Thompson, T.B., 1964, Tectonics and general geology of the Ruidoso-Carrizozo region, central New Mexico: New Mexico
Geological Society, 15th Field Conference Guidebook, p. 110–121.
Kelley, V.C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and Mineral Resources, Memoir 24,
75 p
Kelley, V.C., 1972, Geology of the Fort Sumner sheet, New Mexico: New Mexico Bureau of Mines and Mineral Resources, Bulletin 98, 55 p.
Gile, L.H., Hawley, J.W., and Grossman, R.B., 1981, Soils and geomorphology in the Basin and Range area of Southern New Mexico — Guidebook to the Desert Project: New Mexico Bureau of Mines and Mineral Resources, Memoir 39, 222 p.
Gillette, D.D., Wolberg, D.L., and Hunt, A.P., 1986, Tyrannosaurus Rex from the McRae Formation (Lancian, Upper Cretaceous), Elephant Butte
Reservoir, Sierra County, New Mexico: New Mexico Geological Society, Guidebook 37, p. 235–238.
Grainger, J.R., 1974, Geology of the White Oaks Mining District, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University of New
Mexico, 69 p.
Haines, R.A., 1968, The geology of the White Oaks–Patos Mountain area, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University
of New Mexico.
Hook, S.C., 2010, Flemingostrea elegans, n. sp.: guide fossil to marine, lower Coniacian (Upper Cretaceous) strata of central New Mexico: New
Mexico Geology, v. 32, no. 2, p. 35–57.
Koning, D.J., 2009, Radiocarbon age control for Sacramento Mountain-derived alluvial fan deposits near Alamogordo, New Mexico, and related
geomorphic and sedimentologic interpretations [abstract for 2009 NMGS Spring Meeting]: New Mexico Geology, v. 31, no. 2, p. 46.
Kues, B.S., Lucas, S.G., Kietzke, K., and Mateer, N.J., 1985, Synopsis of Tucumcari Shale, Mesa Rica Sandstone, and Pajarito Shale paleontology,
Cretaceous of east–central New Mexico: New Mexico Geological Society Guidebook, 36th Annual Field Conference, p. 261–281
Lozinsky, R.P., Hunt, A.P., Wolberg, D.L., and Lucas, S.G., 1984, Late Cretaceous (Lancian) dinosaurs from the McRae Formation, Sierra County,
New Mexico: New Mexico Geology, v. 6, p. 72–77.
Lucas, S.G., 1991, Correlation of Triassic strata of the Colorado Plateau and southern High Plains, New Mexico: New Mexico Bureau of Mines
and Mineral Resources, Bulletin 137, p. 47–56.
Lucas, S.G., 2004, The Triassic and Jurassic systems in New Mexico, in Mack, G.H., and Giles, K.A., eds., The Geology of New Mexico, A Geologic History: New Mexico Geological Society, Special Publication 11, p. 137–152.
McManus, C.E.D., and McMillan, N.J., 2002, Subduction or rifting:the Eocene magmas of the Sacramento Mountains, NM: Geological Society
of America Abstracts with Programs, v. 34, no. 6, p. 364.
McLemore, V.T., 2002, The Three Rivers Petroglyph site, Otero County, New Mexico [non peer-reviewed mini-paper]: New Mexico Geological
Society, 53rd Annual Field Conference Guidebook, p. 26–27.
Moore, S.L., Foord, E.E., Meyer, G.A., and Smith, G.W., 1988, Geologic map of the northwestern part of the Mescalero Apache Indian Reservation, Otero County, New Mexico: U.S. Geological Survey Map I-1895, scale 1:24,000.
Moore, S.L., Thompson, T.B., and Foord, E.E., 1991, Structure and igneous rocks of the Ruidoso region, New Mexico: New Mexico Geological
Society Guidebook, 42nd Field Conference, p. 137–145.
Munsell Color, 1994 edition, Munsell soil color charts: New Windsor, N.Y., Kollmorgen Corp., Macbeth Division.
Pertl, D.J., and Cepeda, J.C., 1991, The Carrizo Mountain stock and associated intrusions, Lincoln County, New Mexico: New Mexico Geological
Society Guidebook, 42nd Annual Field Conference, p. 147–152.
Kountz Canyon and Gaylord Peak flows (lower Oligocene?)—The Kountz Canyon flow is a crystal-rich (15–20%) porphyritic flow with distinctive zoned, blocky potassium feldspar phenocrysts that are dark gray at the center and white on the rim. This flow was deposited on a rugged
paleotopography. Up to 25 m thick. The Gaylord Peak flows are porphyritic lavas with potassium feldspar and green pyroxene; the pyroxene
commonly forms in clusters. The feldspar phenocrysts have a bimodal range of grain sizes. Maximum thickness of the flows is 200 m.
Nogal Peak trachyte (lower Oligocene)—Gray, slightly porphyritic to aphyric lavas with intercalated flow breccia, as well as minor volcaniclastic
sediment. Includes an aphanitic to sparsely porphyritic (<2%) lava capping a hill with a spot elevation of 8,594 ft along the Pennsylvania trail. West
and southwest of Nogal Peak, the unit consists of a single flow of gray, slightly porphyritic, medium- to fine-grained lava containing phenocrysts of
plagioclase in a trachytic matrix. 40Ar/39Ar date of 31.41 ± 0.38 Ma was determined from a trachydacite that overlies the “high country” tuff on a
ridge north of Nogal Peak in the headwaters of Norman Canyon. Maximum exposed thickness of flow is ≤35 m.
Church Mountain phonolite (lower Oligocene)—Gray crystal-rich flows containing variable lithic content and sparse pumice. Phenocrysts are
dominantly potassium and plagioclase feldspar with minor biotite and amphibole. Lithics are generally pebble-sized and sparse to absent, but
locally constitute up to 10% of outcrops. Pumice is sparse to absent, fine pebble in size, and flattened. Included in this unit are interbedded volcaniclastic sediments and fine grained lava flows. Samples submitted for radiometric analyses from bottom and top of unit returned 40Ar/39Ar ages of
32.70 ± 0.10 Ma and 32.72 ± 0.16 Ma, respectively. Biotite from the lower sample returned a 40Ar/39Ar age of 32.95 ± 0.12 Ma.
Three Rivers Formation, undivided (upper Eocene, possibly lower Oligocene)—From youngest to oldest, includes the Buck Pasture, Double
Diamond, Argentina Spring Tuff, Taylor Well, and Rattlesnake Canyon members.
Buck Pasture Tuff Member of Three Rivers Formation (upper Eocene)—Welded to unwe ded h c ch u The h c agmen s a e angu a
p eces o achy c avas The phenoc ys s a e san d ne p ag oc ase b o e and py oxene The u con a ns ma c c o s ha a e a ened nea he
base and ha a e ounded o embayed bu mo e equan upsec on n p aces a h n bed o h c bea ng u s m a o he Buck Pas u e Tu s
p ese ved abou 15–20 m be ow he ma n exposu es 40A /39A san d ne da e s 34 28 ± 0 05 Ma on exposu es n he God ey H s The “h gh
coun y” u ove a n by Noga Peak T achy e on Noga Peak s s m a o he exposu es n he God ey H s and s n e bedded n he Doub e
D amond Fo ma on 0–60 m h ck
Doub e D amond Member o Three R vers Forma on uppe Eocene poss b y owe O gocene — n e ca a ed p ag oc ase phy c po phy y
avas p ag oc ase and amph bo e phy c po phy y avas and pebb e o oca y bou de cong ome a es A achyandes e a Sp ng Po n ha s
us above A gen na Sp ng Tu gave a 40A /39A da e o 35 32 ± 0 16 Ma Up o ~280 m h ck n he a ea o D amond Peak
Argen na Spr ngs Tu Member o he Three R vers Forma on uppe Eocene —A h c ch p ag oc ase phy c ow o a ed heomo ph c
gn mb e The gn mb e n e va s a e b ack o g ay o ye ow sh an s gh y we ded o dense y we ded and h c ch w h a ened pum ce
amme w h a max mum aspec a o o ≥25 1 L h c agmen s cons s o wh e che o ne g a ned sands one and a va e y o gh o da k co
o ed vo can c ocks nc ud ng syen c ocks The e appea s o be a vo can c as c sed men a y n e va be ween wo zones o s ong y o a ed
h c ch gn mb e 40A /39A da e s 36 06 ± 0 70 Ma Un s 40–120 m h ck
Spr ng Canyon rachydac e uppe Eocene –Th ck c o m ng ava o aphy c ow banded achydac e Con a ns ve y spa se sma
phenoc ys s o p ag oc ase n a e y g oundmass o ny p ag oc ase c nopy oxene b o e and magne e some spec mans a e spo ed w h c o s
o ny p ag oc ase Fo me y ca ed " achyandes e o Sp ng Canyon" by Thompson 1972 1973 Max mum exposed h ckness nea ven s 110
m
Tay or We Member o he Three R vers Forma on uppe Eocene —Da k g ay ne g a ned 1–4 m h ck ava ows cha ac e zed by a s ve y
sheen and sp o ches on wea he ed su aces F ows a e d scon nuous and a e n e ca a ed w h ed a e ed vo can c as c sed men a y ocks A
achybasa n h s un has an mp ec se 40A /39A da e o 3784 ± 0 48 Ma The op o he Tay o We Membe on he S e a B anca mass
con a ns a h ck ex ens ve ow he Sp ng Canyon achydac e 40A /39A 36 87 ± 0 13 Ma ha s pe o og ca y and chem ca y d s nc om
unde y ng s a a To a h ckness up o 365 m
Ra esnake Member o he Three R vers Forma on uppe Eocene —Da k g ay po phy c achyandes e w h phenoc ys s o p ag oc ase and
py oxene p ag oc ase s he dom nan phenoc ys The avas a e va ab y c ys a poo 5% o c ys a ch 30% The basa con ac w h he unde
y ng Hog Pen Fo ma on vo can c b ecc a s g ada ona The con ac be ween he p ag oc ase phy c achyandes e and he achybasa un s s
oca y ma ked by a d s nc ve c ys a ch ava ow w h a ge 1–2 cm e onga e p ag oc ase a hs 150 m h ck
Hog Pen Forma on m dd e? o uppe Eocene —G een o ed vo can c as c o vo can c un con a n ng ow b ecc a deb s ows mud ows ava
ows and ed sands one o sandy cong ome a e The ow b ecc a c as s and ava ows a e composed p ma y o po phy c basa c
achyandes e o achybasa w h phenoc ys s o py oxene and p ag oc ase he py oxene phenoc ys s a e usua y >5 mm and a e no ceab e on
wea he ed su aces Typ ca deb s ow c as s a e 5 o 20 cm n d ame e a hough some a e >1 m ac oss 40A /39A ho nb ende da es om nea
he base o he un a e 36 57 ± 0 21 o 3701 ± 0 10 Ma 120–180 m
Sanders Canyon Forma on m dd e Eocene — n e bedded edd sh g ay o edd sh b own oodp a n depos s and gh g ay sandy channe s
The ave age sands one/muds one a o o h s uv a un s abou 30 70 Ca he 1991 and dec eases up sec on The un appears o be
ner gra ned wes o Cub Moun a n han s o he sou heas A hough ongues o h s o ma on a e n e bedded n he Cub Moun a n Fo ma
on h s un s on y mapped whe e ove es he en e Cub Moun a n Fo ma on Channe s occupy vague abu a beds <35 cm h ck and
con a n up o 1% pebb es and esse cobb es bou de s o p ag oc ase phy c andes e Sands one pe o og c s udy by Ca he 1991 g ves anges
o 31–65% vo can c ock agmen s nc ud ng 0 5–2% b o e g a ns 8–41% w nned p ag oc ase 7–31% qua z dec eas ng up sec on 0–7%
m c o ne and o hoc ase 0–4% g an e and gne ss ock agmen s 0–3% che 0–2% me amo ph c ock agmen s and 0–2% sands one ock
agmen s F oodp a n sed men cons s s o c ays one s s one muds one and ve y ne o ne g a ned sands one Gene a y he basa mapped
con ac s p obab y con o mab e No h o Ba be R dge he uppe 50–100 m o h s un cons s s o gh g ay o ma oon gene a y mass ve
muds one and c ayey s y ve y ne o ne g a ned sands one Un s sha p y and egu a y ove a n by vo can c cong ome a es o he Hog Pen
Fo ma on Twh We o mode a e y conso da ed and weak y cemen ed by ca c um ca bona e gene a y a s ope o me Abou 120 m o h s un
s exposed no hwes o Noga Peak bu he o a h ckness he e may poss b y be as much as 400 m Un h ns o he sou h and s no obse ved
sou h o he Th ee R ve s d a nage
Cub Moun a n Forma on owe o m dd e Eocene —Wh e o pa e ye ow o gh edd sh g ay a kos c channe
sands ones n e bedded w h
ed edd sh b own o edd sh p nk sh g ay oodp a n depos s o muds one and ve y ne o ne g a ned sands one Sands one pe o og c s udy
by Ca he 1991 g ves anges o 50–70% qua z 3–15% m c o ne and o hoc ase 2–16% g an e and gne ss ock agmen s 5–11% vo can c
ock agmen s 1–9% che 0–9% me amo ph c ock agmen s 0 5–6% w nned p ag oc ase and 0–3% sands one ock agmen s Loca y ve y
coa se sand and pebb es a e p esen n he channe s composed o qua z + qua z e hyo e and che F oodp a n depos s cons s o
c ays one muds one s s one and ve y ne o ne g a ned sands one The s gh y coa se ex u e o he sand mos y med um g a ned mo e
“pocke y” ou c op appea ance and edd sh ne g a ned sands one beds se ve o d s ngu sh h s uv a un om he unde y ng C evasse Canyon
Fo ma on The un d e s om he ove y ng Sande s Canyon Fo ma on by s gene a ack o gh g ay channe s and esse amoun s o vo can c
de us n s sand ac on ess han 20% Loca y he e a e und e en a ed ongues o Sande s Canyon Fo ma on n he m dd e o uppe pa o
he Cub Moun a n Fo ma on These ongues a e yp ca y composed o gh g ay ne o med um g a ned sands one ha have 20% h c
agmen s + ma c g a ns nc ud ng abundan b o e Base o un de ned a he op o he pa eoso deve oped on he unde y ng C evasse
Canyon Fo ma on desc bed be ow Th ckness ange o 370–570 m
Crevasse Canyon Forma on Uppe C e aceous — n e ca a ed channe
sands ones and oodp a n depos s Th s uv a sed men d e s om
he ove y ng Cub Moun a n Fo ma on by s ye ow sh g een sh oodp a n depos s and s gh y ne sand n channe s Un coa sens up sec on
Uppe 250–270 m o un con a ns ~ subequa ±20% sands one–muds one Sands one s wh e o pa e ye ow o o ve ye ow o gh g ay
common y wea he ng o ye ow o ange and ne o coa se g a ned mos y ne o med um g a ned excep n he uppe pa o he un Chan
ne pebb es occu nea op o un Coa se channe s a e mos y cemen ed by ca c um ca bona e Ca he 1991 F oodp a n sed men cons s s
o muds one s s one and ve y ne o ne g a ned sands one coa seams a e oca y common and gene a y up o 30 cm h ck Uppe con ac
mapped a he op o a d s nc ve 3–8 m h ck pa eoso s composed o a gh g ay o gh g ay sh g een mass ve b o u ba ed sands one w h
10–15% egu a da k pu p e o pu p sh b ack conc e ons o manganese ox de ?
Trans ona erres r a –mar ne un n he ower Crevasse Canyon Forma on Uppe C e aceous Con ac an S age —Lowe 18–28 m cons s s
o n e bedded g ay sha e and m no ye ow sands one and coa beds h s s co e a ed o he D co Membe C evasse Canyon Fo ma on
Uppe 24–45 m s co e a ed o he Da on Sands one C evasse Canyon Fo ma on
s composed p ma y o pa e ye ow ne o med
um g a ned sands one ha oca y con a ns ma ne nve eb a e oss s nc ud ng oys e s Base o Da on Sands one con a ns hummocky c oss s a
ca on 1 m h ck o ess unde a n by ~1 m o b o u ba ed sands one Top con ac s d awn a he uppe mos h ck ca ca eous o ang sh
ne g a ned sands one o sandy mes one bed con a n ng she oss s nc ud ng oys e s Lowe con ac s d awn a he owe mos occu ence o
coa Coa s se dom exposed so base s common y d awn us above he opmos edge o Ga up Sands one 40–70 m h ck
Ga up Sands one Uppe C e aceous owe Con ac an S age —Nea sho e sands one ongues n e bedded w h gh g ay o g ay ss e ma ne
sha e n e va s n a g ven sands one ongue s a a p og ess upwa ds om 1–2 m o b o u ba ed sand o 1–2 m o hummocky c oss s a ed sand
o seve a me e s o angen a c oss s a ed up o 60 cm h ck o ese s and ho zon a p ana am na ed sand Sand s wh e o pa e ye ow o
ye ow and ve y ne o med um g a ned mos y ne o med um g a ned Top o sands one beds oca y con a n pa eo bu ows Oys e she s a e
abundan oca y The op bed o he uppe sands one ongue unde y ng he coa bea ng D co Membe o he C evasse Canyon Fo ma on s
gene a y h ck abu a and composed o a d s nc ve ne o med um g a ned b o u ba ed qua zose sands one Base o un g ades downwa d
n o he D C oss Tongue o he Mancos Sha e basa con ac d awn a he bo om o he owes 2 m h ck o g ea e sands one ongue d sp ay ng
he a o emen oned sha ow ng upwa d cyc e Deg ee o cemen a on s h gh y va ab e An oys e ca ed F em ngos ea e egans s un que o he
Ga up Sands one and con ms hos a g aph c co e a ons o h s o ma on Hook 2010 100–130 m h ck
Mancos Sha e und v ded Uppe C e aceous m dd e Cenoman an ? o owes Con ac an S age —G ay o gh g ay o gh o ve g ay ss e
sha e Me amo phosed o a b ack o g ay a g e ad acen o acco hs
Mancos Sha e D Cross Tongue Member Uppe C e aceous m dd e Tu on an o owes Con ac an S age —Da k g ay o g een sh g ay o pa e
ye ow ss e sha e s y sha e s s one and c ays one S gh o no e e vescence n hyd och o c ac d T ace o common s de e and/o ca c um
ca bona e cemen ed conc e ons ha a e up o 0 5 m n d ame e Un e odes ead y Towa d op o un g een o b own beds o s s one and
ve y ne o ne g a ned sands one become p og ess ve y mo e common Sha e s me amo phosed o a b ack o g ay a g e mmed a e y
ad acen o acco hs o d kes Un s g ada ona y ove a n by he Ga up Sands one and unde a n by he T es He manos Fo ma on 100–120
m h ck
Lower ongue o Mancos Sha e uppe C e aceous m dd e Cenoman an o m dd e Tu on an S age —Ha d ca ca eous sha e g ay o ve y da k
g ay wea he ng o g ay o gh g ay o gh ye ow sh b own Lowe pa o un nc udes seve a ben on e aye s Up sec on s an n e va o h ee
c ose y spaced med um o h ck bedded <50 cm h ck abu a mes ones ha a e da k g ay wea he ng o gh g ay and m c c These
mes ones a e sepa a ed by ess han 1 m o sha e and co e a ed w h he Br dge Creek L mes one beds Un s g ada ona y ove a n by he
T es He manos Fo ma on The basa Mancos Sha e con a ns h n sands one beds and g ades downwa d n o he Dako a Sands one 100 m ?
h ck
Tres Hermanos Forma on uppe C e aceous m dd e Tu on an S age —A ongue o ve y ne o med um g a ned mos y ne g a ned sands one
w h n he Mancos Sha e oca y con a n ng she deb s and che agmen s Co o s ange om pa e ye ow o gh g ay wea he ng o b own
sh ye ow ve y pa e b own o pa e ye ow Sands one s oca y n e bedded w h subo d na e ye ow sha e beds n p aces enses o b o u ba ed
ye ow sh b own sands one occu ha nc ude oys e b va ve and ammon e emnan s Loca y bu ows a e obse ved A p ano convex med
um s zed bbed oys e ca ed Came eo opha be ap ca a con ms hos a g aph c co e a ons w h he T es He manos Fo ma on Hook and
Cobban 2011 and Hook n p ess 10–60 m h ck h nn ng o he no heas
Dako a Sands one uppe C e aceous Cenoman an ? S age —Ledge o m ng ne o coa se g a ned qua z a en e sands one F esh co o s
ange om wh e o gh pu p sh wh e Exposed sands one ends o deve op a s ong pu p sh b ack o da k b own dese va n sh M no <15%
n e beds o gh g ay s s one Ve y ne o ve y coa se pebb e cong ome a e beds occu nea he base o un ~1% es ma ed vo ume as ve y
h n o med um enses Coa se o ve y coa se g a ned sand s mo e common nea he base o he un bu s ess han 10% o vo ume Coa se
sand g a ns and pebb es a e composed o ounded qua z e qua z che and 0 5–1% me a hyo e n e beds o gh g ay s s one ve y
ne g a ned sands one and gh o da k g ay sha e become nc eas ng y common up sec on Uppe mos sands one beds a e ex ens ve y
bu owed and nc ude Oph omorpha The owe con ac s a scou ed uncon o m y oca y ng pa eova eys and he uppe con ac g ades
con o mab y n o he owe ongue o he Mancos Sha e Top con ac p aced a op o uppe qua z a en e sands one w h Oph omorpha
bu ows Sands one beds a e we cemen ed Mos y 35–50 m h ck bu h ckness va ues o 60 m epo ed by Sm h 1964 and Ha nes 1968
Tr ass c und v ded—Mapped n he subsu ace n he Ca zozo a ea whe e T ass c o ma ons younge han he Moenkop may be p esen
Moenkop Forma on m dd e T ass c owe An s an S age —Choco a e b own o edd sh b own uv a n e bedded sands one and pebb y
sands one channe s and oodp a n depos s Ex a o ma ona c as s a e composed o qua z che qua z e and me a hyo e ? spa se
n a o ma ona c as s a e composed o mes one Sand s gene a y a ha en e w h va ab e m ca con en Bo h sands one and cong ome a e
beds equen y con a n mud p up c as s F oodp a n depos s a e composed o muds one s s one and ve y ne o ne g a ned sands one Lowe
con ac s a p ana o scou ed uncon o m y ove he A es a G oup scou e e o 1–3 m Uncon o mab y ove a n by he Dako a Sands one
App ox ma e y 30–70 m h ck
Grayburg Forma on Ar es a Group uppe Pe m an uppe Guada up an No h Ame can S age —Ve y ne o ne g a ned qua z a en e
sands one and s y o c ayey ve y ne o ne g a ned sands one subo d na e s s one and sha e Co o s ange om o ange o ed o gh ed o
edd sh b own mos o eas common Common y b o u ba ed a hough ve y oca y am na ons and pp e ma ks can be obse ved Reduc on
b eached spo s 0 5–2 mm n d ame e cove 1–15% o ock a ea w h h ghe cove age a ong bedd ng and au p anes whe e hey a e dec me
e sca e and egu a No oss s obse ved Th ck gypsum o anhyd e beds a e absen o he no h bu nc ease o he sou h o abou 5–10% o
he un mo e common owa d he op O ang sh co o ne ex u e and qua z a en e compos on se ve o d e en a e h s un om he ove y ng
Moenkop Fo ma on Lowe con ac w h San And es Fo ma on s a d scon o m y F gure 3 We s nea Th ee R ve s nd ca e a h ckness o
90–110 m a hough o he no h he un may be 130 m h ck
San Andres Forma on und v ded owe o uppe Pe m an Leona d an o Guada up an No h Ame can S age —Und v ded mes one do om e
and anhyd e s a a Do om e and anhyd e a e mo e common up sec on Un depos ed n a sha ow ma ne se ng The San And es Fo ma on
was genera y subd v ded n o he Fourm e Draw Member he Hondo Sands one and he R o Bon o Member hese un s a e desc bed
be ow 240–250 m h ck based on subsu ace da a o we s n he Th ee R ve s a ea
Py
Fourm e Draw Member uppe Pe m an Guada up an No h Ame can S age —M c c da k g ay mes one g ay sh an o gh g ay
do om e and gypsum o anhyd e Beds a e med um o h ck and abu a Ca bona es become mo e do om c up sec on and he p opo
on o evapo e beds nc eases up sec on Base o membe d awn a he owes anhyd e bed Loca pa eoka s b ecc as App ox ma e y
100–120 m h ck
Hondo Member uppe Pe m an Guada up an No h Ame can S age —Tann sh wh e o ye ow sh an ne o med um g a ned qua zose
sands one Less han 5 m h ck
R o Bon o Member uppe Pe m an Guada up an No h Ame can S age —Med um o da k g ay gene a y m c c mes one and m no
do om e Bedd ng s h n o h ck and abu a Th ck bed s o ann sh wh e o ye ow sh an ne o med um g a ned qua zose sands one
up o 2 m h ck s p esen nea op 3–10 m be ow uppe con ac and base o un co e a ed o he Hondo Sands one Un depos ed n
a sha ow ma ne se ng ~ 60 m h ck
Yeso Forma on owe Pe m an —Ve y pa e edd sh b own o gh b own and composed p edom nan y o gypsum w h m no mes one/do om e
Gypsum s a n y am na ed n p aces hough bedd ng s usua y con o ed L mes one beds a e ess han 0 3 m h ck a e da k b own g ay n co o
and appea o be n ense y b o u ba ed No oss s we e obse ved Th ckness no we cons a ned bu poss b y up o 300 m
Lopez Spring Formation, undivided (lower Oligocene)—Interval of thin to thick (1–10 m) discontinuous trachyte, porphyritic trachyandesite,
Tgl
Stearns,
C.E.,trachydacite,
1953, Tertiary
of the
Galisteo-Tonque
area, New
Mexico: Geological
of America
Bulletin, v. 64,
p. 459–508.
biotite
and geology
trachybasalt
flows
complexly intercalated
with volcaniclastic
sediments. Society
Some exposures
of volcaniclastic
sediment
are
dominated by biotite-bearing trachydacite clasts. Unit includes a thick (up to 85 m) flow of fine-grained trachyandesite in the southeastern Godfrey
Tait, D.B.,
Ahlen,
J.L., Gordon,
A., Scott, of
G.L.,
Motts, W.S.,
Spitler,
M.E.,
1962,
Artesia Group
of New
Mexico
andinwest
Texas: Bulletin
of the AmeriHills,
containing
small phenocrysts
hornblende,
pyroxene,
and
clusters
of potassium
feldspar.
Irregular
base fills
paleovalleys.
Radiometric
40
can Association
of Petroleum
vol.± 46,
p. 504–517.
Ar/39ArGeologists:
ages of 31.05
0.76no.
Ma4,and
30.04 ± 0.2 Ma (the latter is from a trachydacite cobble in volcaniclastic sediments).
dating returned
200–220(?) m thick.
Thompson, T.B., 1964, A stratigraphic section of the Sierra Blanca Volcanics in the Nogal Peak area, Lincoln County, New Mexico: New Mexico
Canyon15th
and Field
Gaylord
Peak flowsp.(lower
Oligocene?)—The Kountz Canyon flow is a crystal-rich (15–20%) porphyritic flow with distincTkgf Kountz
Geological
Society,
Conference,
76–78.
tive zoned, blocky potassium feldspar phenocrysts that are dark gray at the center and white on the rim. This flow was deposited on a rugged
paleotopography. Up to 25 m thick. The Gaylord Peak flows are porphyritic lavas with potassium feldspar and green pyroxene; the pyroxene
Thompson,
T.B., 1966, Geology of the Sierra Blanca, Lincoln and Otero Counties, New Mexico [Ph.D. dissertation]: Albuquerque, University of
commonly forms in clusters. The feldspar phenocrysts have a bimodal range of grain sizes. Maximum thickness of the flows is 200 m.
New Mexico, 146 p.
Tnpt
Nogal Peak trachyte (lower Oligocene)—Gray, slightly porphyritic to aphyric lavas with intercalated flow breccia, as well as minor volcaniclastic
Thompson,
T.B., Includes
1972, Sierra
Blanca
complex, (<2%)
New Mexico:
Geological
of America
Bulletin,
v. the
83,Pennsylvania
p. 2,341–2,356.
sediment.
an aphanitic
to igneous
sparsely porphyritic
lava capping
a hill with aSociety
spot elevation
of 8,594
ft along
trail. West
and southwest of Nogal Peak, the unit consists of a single flow of gray, slightly porphyritic, medium- to fine-grained lava containing phenocrysts of
40
Ar/
Ar date and
of 31.41
± 0.38
Ma districts,
was determined
from a trachydacite
that of
overlies
“high
country”
tuff on a Circuplagioclase
in a trachytic
Thompson,
T.B., 1973.
Mineralmatrix.
deposits
of39Nogal
Bonito
mining
New Mexico:
N.M. Bureau
Minestheand
Mineral
Resources,
of Nogal
Peak in map.
the headwaters of Norman Canyon. Maximum exposed thickness of flow is ≤35 m.
lar 123,ridge
29 north
p. w/color
geologic
Mountain phonolite (lower Oligocene)—Gray crystal-rich flows containing variable lithic content and sparse pumice. Phenocrysts are
Tcp Church
Udden,
J.A., 1914,
The mechanical composition of clastic sediments: Bulletin of the Geological Society of America, v. 25, p. 655–744.
dominantly potassium and plagioclase feldspar with minor biotite and amphibole. Lithics are generally pebble-sized and sparse to absent, but
locally constitute up to 10% of outcrops. Pumice is sparse to absent, fine pebble in size, and flattened. Included in this unit are interbedded volcaniWaresback,
D.B., 1986,
Formation,
New
Mexico
– analysis
of a continental
volcaniclastic
alluvial
fan 40sequence
[unpublished
Ar/39Ar ages
of
clastic sediments
andThe
finePuye
grained
lava flows.
Samples
submitted
for radiometric
analysesrift-filling
from bottom
and top of unit
returned
40
39
M.S. thesis]:
Arlington,
University
of
Texas,
225
p.
32.70 ± 0.10 Ma and 32.72 ± 0.16 Ma, respectively. Biotite from the lower sample returned a Ar/ Ar age of 32.95 ± 0.12 Ma.
Waresback,
D.B.,
and Turbeville, B.N., 1990, Evolution of a Pliocene-Pleistocene volcanogenic alluvial fan – the Puye Formation, Jemez MounWALKER
GROUP
tains, New Mexico: Geological Society of America Bulletin, v. 102, p. 298–314.
Three Rivers Formation, undivided (upper Eocene, possibly lower Oligocene)—From youngest to oldest, includes the Buck Pasture, Double
Argentina
Spring
Tuff,
Taylor Well,
and Rattlesnake
Canyon New
members.
Weber,Diamond,
R.H., 1964,
Geology
of the
Carrizozo
quadrangle,
New Mexico:
Mexico Geological Society, 15th Field Conference Guidebook,
Twt
Smith, C.T., 1964, Reconnaissance geology of the Little Black Peak Quadrangle, Lincoln and Socorro Counties, New Mexico: New Mexico
Institute of Mining and Technology, State Bureau of Mines and Mineral Resources, Circular 75.
Buck Pasture Tuff Member of Three Rivers Formation (upper Eocene)—Welded to unwelded lithic-rich tuff. The lithic fragments are angular
pieces of trachytic lavas. The phenocrysts are sanidine, plagioclase, biotite, and pyroxene. The tuff contains mafic clots that are flattened near the
Wentworth,
C.K.,that
1922,
A scaletoofembayed,
grade and
forupsection.
clastic sediments:
ofofGeology,
v. 30,
377–392.
base and
are rounded
butclass
more terms
equant,
In places aJournal
thin bed
lithic-bearing
tuffp.similar
to the Buck Pasture Tuff is
preserved about 15–20 m below the main exposures. 40Ar/39Ar sanidine date is 34.28 ± 0.05 Ma on exposures in the Godfrey Hills. The “high
Williams,
H., Turner,
F.J., and
C.M.,
1954.onPetrography.
Freeman
& Co., San
Francisco,
p. is interbedded in the Double
country”
tuff overlain
by Gilbert,
Nogal Peak
Trachyte
Nogal Peak W.H.
is similar
to the exposures
in the
Godfrey 406
Hills and
Diamond Formation. 0–60 m thick.
Soil Survey Staff, 1992, Keys to Soil Taxonomy: U.S. Department of Agriculture, SMSS Technical Monograph no. 19, 5th edition, 541 p.
Wolberg, D.L., Lozinsky, R.P., and Hunt, A.P., 1986, Late Cretaceous (Maastrichtian–Lancian) vertebrate paleontology of the McRae Formation,
Member
of Three
Rivers Formation
(upperGeological
Eocene, possibly
lower
Oligocene)—Intercalated
plagioclase-phyric porphyry
Twtd Double
Elephant
Butte Diamond
area, Sierra
County,
New Mexico:
New Mexico
Society,
Guidebook
37, p. 227–234.
Twbpt
lavas, plagioclase- and amphibole-phyric porphyry lavas, and pebble to locally boulder conglomerates. A trachyandesite at Spring Point that is
just above Argentina Spring Tuff gave a 40Ar/39Ar date of 35.32 ± 0.16 Ma. Up to ~280 m thick in the area of Diamond Peak.
Stearns, C.E., 1953, Tertiary geology of the Galisteo-Tonque area, New Mexico: Geological Society of America Bulletin, v. 64, p. 459–508.
Tait, D.B., Ahlen, J.L., Gordon, A., Scott, G.L., Motts, W.S., Spitler, M.E., 1962, Artesia Group of New Mexico and west Texas: Bulletin of the American Association of Petroleum Geologists: vol. 46, no. 4, p. 504–517.
Lopez Spring Formation, undivided (lower Oligocene)—Interval of thin to thick (1–10 m) discontinuous trachyte, porphyritic trachyandesite,
biotite trachydacite, and trachybasalt flows complexly intercalated with volcaniclastic sediments. Some exposures of volcaniclastic sediment are
dominated by biotite-bearing trachydacite clasts. Unit includes a thick (up to 85 m) flow of fine-grained trachyandesite in the southeastern Godfrey
Hills, containing small phenocrysts of hornblende, pyroxene, and clusters of potassium feldspar. Irregular base fills in paleovalleys. Radiometric
dating returned 40Ar/39Ar ages of 31.05 ± 0.76 Ma and 30.04 ± 0.2 Ma (the latter is from a trachydacite cobble in volcaniclastic sediments).
200–220(?) m thick.
and flow breccias of trachydacite with ~10% phenocrysts of plagioclase, biotite, and pyroxene. 40Ar/39Ar date is 28.78 ± 0.04 Ma. 60–70 m
thick.
p. 100–109.
Rawling, G.C., 2011, Geology of the Capitan and Nogal quadrangles, Lincoln County, New Mexico: New Mexico Bureau of Geology and
Mineral Resources, Open-file Report 538, scale 1:24,000.
Biotite trachydacite flow of the Jackass Mountain Formation (lower Oligocene)—Cliff-forming succession of light gray flow-banded lava flows
and flow breccias of trachydacite with ~10% phenocrysts of plagioclase, biotite, and pyroxene. 40Ar/39Ar date is 28.78 ± 0.04 Ma. 60–70 m
thick.
Psr
taphony weathering texture. Contains <2% lithic fragments composed of trachyandesite and trachyte lavas. Phenocrysts include plagioclase,
Rawling,
G.C., pyroxene,
2011, Geology
of the
and and
Nogal
quadrangles,
County,
New Mexico:
Newwelded
Mexico
Bureau
Geology and
sanidine,
magnetite,
and Capitan
sparse biotite
hornblende.
The tuffLincoln
is generally
crystal-poor,
but the more
intervals
areof15–20%
Mineralphenocrysts.
Resources,40Open-file
Report
538,±scale
Ar/39Ar ages
of 28.67
0.07 1:24,000.
Ma and 28.66 ± 0.08 Ma were obtained from sanidine in the tuff. Geochemically, this tuff is a
Haines, R.A., 1968, The geology of the White Oaks–Patos Mountain area, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University
of New Mexico.
Cather, S.M., 1991, Stratigraphy and provenance of upper Cretaceous and Paleogene strata of the western Sierra Blanca Basin, New Mexico:
New Mexico Geological Society Guidebook, 42nd Field Conference, p. 265–275.
Palisades Tuff Member of the Jackass Mountain Formation (lower Oligocene)—Cliff-forming welded tuff with pronounced eutaxitic foliation and
taphony weathering texture. Contains <2% lithic fragments composed of trachyandesite and trachyte lavas. Phenocrysts include plagioclase,
sanidine, pyroxene, magnetite, and sparse biotite and hornblende. The tuff is generally crystal-poor, but the more welded intervals are 15–20%
phenocrysts. 40Ar/39Ar ages of 28.67 ± 0.07 Ma and 28.66 ± 0.08 Ma were obtained from sanidine in the tuff. Geochemically, this tuff is a
trachyte. 25–90 m thick.
Psh
Pertl, D.J., and Cepeda, J.C., 1991, The Carrizo Mountain stock and associated intrusions, Lincoln County, New Mexico: New Mexico Geological
120000
SocietyPalisades
Guidebook,
42nd Annual Field Conference, p. 147–152.
Tuff Member of the Jackass Mountain Formation (lower Oligocene)—Cliff-forming welded tuff with pronounced eutaxitic foliation and
Allen, M.S., and Foord, E.E., 1991, Geological, geochemical and isotopic characteristics of the Lincoln County porphyry belt: implications for
regional tectonics and mineral deposits: New Mexico Geological Society Guidebook 42, p. 97–113.
Hook, S.C., and Cobban, W.A., 2011, The Late Cretaceous oyster Cameleolopha bellaplicata (Shumard 1860), guide fossil to middle Turonian
strata in New Mexico: New Mexico Geology, v. 33, no. 3, p. 67–96.
Brecciated, porphyritic trachyte of the Jackass Mountain Formation (lower Oligocene)—Light gray trachyte lava flows with phenocrysts of
sanidine and pyroxene interbedded with monolithologic breccia with subround to angular clasts in a light gray matrix. 40Ar/39Ar ages of 28.59 ±
0.05 Ma and 28.53 ± 0.03 Ma were obtained from sanidine in the unit. Trachyte lava flows that are similar to Tgjb flows are present between
Godfrey Peak and Maverick Spring, but this lava contains biotite in addition to sanidine and pyroxene. This lava is separated from the overlying
Tgjb flows by a distinct, mappable flow break. 60–140 m thick.
Psf
sanidine andKclt
pyroxene interbedded with monolithologic2000
breccia with subround to angular clasts in a light gray matrix. 40Ar/39Ar ages of 28.59 ±
Ma 1994
and 28.53
± 0.03
Ma were
obtained
fromNew
sanidine
in the unit.
Trachyte
lava flows
that Macbeth
are similar Division.
to Tgjb flows are present between
Munsell0.05
Color,
edition,
Munsell
soil color
charts:
Windsor,
N.Y.,
Kollmorgen
Corp.,
Kg
1000biotite in addition to sanidine and pyroxene. This lava is separated from the overlying
Godfrey Peak
Kt and Maverick Spring, but this lava contains
Kml
Tgjb flows
by Kd
a distinct, mappable flow break. 60–1400m thick.
Trm
REFERENCES
Lucas, S.G., Lueth, V.W., Kues, B.S., Myers, R.G., and Giles, K.A., 2002, First-day road log, from Alamogordo to Tularosa, Mockingbird Gap, Trinity
Site, Oscuro, and Three Rivers: New Mexico Geological Society Guidebook, 53rd Annual Field Conference, p. 20.
Biotite trachyte within trachyte to trachyandesite flows of the Jackass Mountain Formation (lower Oligocene)—Flow of trachydacite with
biotite set in a sugary matrix interbedded with Tgjta. At one locality on the east side of Jackass Mountain, this unit consists of altered tephra (< 1
cm) overlain by an ignimbrite with feldspar, altered mafics, and granular-sized rock fragments. 40Ar/39Ar date is 28.60 ± 0.05 Ma. 1–10 m thick.
Moore, S.L., Thompson, T.B., and Foord, E.E., 1991, Structure and igneous rocks of the Ruidoso region, New Mexico: New Mexico Geological
3000 Formation (lower Oligocene)—Light gray trachyte lava flows with phenocrysts of
Kcporphyritic
Society
Guidebook,
42nd Field
Conference,
p. 137–145.
trachyte
of the Jackass
Mountain
Tgjb Brecciated,
Smith, C.T., 1964, Reconnaissance geology of the Little Black Peak Quadrangle, Lincoln and Socorro Counties, New Mexico: New Mexico
trachydacite
flow of theState
Jackass
Mountain
Formation
(lower Oligocene)—Cliff-forming
Tgjt Biotite
Institute
of Mining
and Technology,
Bureau
of Mines
and Mineral
Resources, Circular 75.succession of light gray flow-banded lava flows
Broadhead, R., and Jones, G., 2004, Oil, natural gas, and helium potential of the Chupadera Mesa area, Lincoln and Socorro Counties, New
Mexico: New Mexico Bureau of Geology and Mineral Resources, Open-file Report 478.
Trachyte to trachyandesite flows of the Jackass Mountain Formation (lower Oligocene)—Light to dark gray fine-grained lava with a trachytic
texture and contorted platy flow foliation. The unit is composed of a series of thin flows 1–10 m thick with basal scoriaceous breccia and vesicular
flow tops with elongated vesicles. Red to yellow alteration of the flow breaks is common. 50 m thick.
40
39
cm) overlain by an ignimbrite with feldspar, altered mafics,
4000and granular-sized rock fragments. Ar/ Ar date is 28.60 ± 0.05 Ma. 1–10 m thick.
Lozinsky, R.P., Hunt, A.P., Wolberg, D.L., and Lucas, S.G., 1984, Late Cretaceous (Lancian) dinosaurs from the McRae Formation, Sierra County,
New Mexico: New Mexico Geology, v. 6, p. 72–77.
Hook, S.C., Cobban, W.A., 2007, A condensed middle Cenomanian succession in the Dakota Sandstone (upper Cretaceous), Sevilleta National
Wildlife Refuge, Socorro County, New Mexico: New Mexico Geology, vol. 29, no. 3, p. 75–99.
Ps
flow tops with elongated vesicles. Red to yellow alteration of the flow breaks is common. 50 m thick.
Grainger, J.R., 1974, Geology of the White Oaks Mining District, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University of New
Mexico, 69 p.
Lucas, S.G., Cather, S.M., Sealey, P., and Hutchison, J.H., 1989, Stratigraphy, paleontology, and depositional systems of the Eocene Cub Mountain
Formation, Lincoln County, New Mexico – a preliminary report: New Mexico Geology, v. 11, p. 11–17.
Pag
Elevation
Lucas, S.G.,
Lueth, V.W., Kues, B.S., Myers,
R.G., and Giles,
K.A., 2002, First-day road log, from Alamogordo to Tularosa, Mockingbird Gap, Trinity
upper Jackass Mountain
Tgjvs Volcaniclastic sediment of theNortheast
(ft)Formation (lower to upper Oligocene)—Consists of a lower and an upper unit. The
Site, Oscuro,
and
Three
Rivers:
New
Mexico
Geological
Society
Guidebook,
53rd
Annual
Field
Conference,
upper unit is a heterolithic landslide deposit with a white ashy matrix
that contains
large
(1–5 m)
angular
boulders p.
of 20.
porphyritic trachyandesite,
Tsts
Twh
^m
Jackass Mountain Formation and the 28.8 to 34.3 Ma Lopez Spring Formation.
spring discharges from
volcaniclastic rock 670
m to NW
Gile, L.H., Hawley, J.W., and Grossman, R.B., 1981, Soils and geomorphology
in the Basin60000
and Range area of Southern New Mexico — GuidePa
70000
40000
50000
book to the Desert Project: New Mexico Bureau of Mines and Mineral Resources, Memoir 39, 222 p.
Py
Lucas, S.G., Cather, S.M., Sealey, P., and Hutchison, J.H., 1989, Stratigraphy, paleontology, and depositional systems of the Eocene Cub Mountain
This unit
appears
to overlie
an unconformity
developed
at about
the Mexico
stratigraphic
level of v.the11,Bucky
Pasture Tuff. Includes the 28.2 to 28.8 Ma
Formation,
Lincoln
County,
New Mexico
– a preliminary
report:
New
Geology,
p. 11–17.
trachyte. 25–90 m thick.
Birkeland, P.W., 1999, Soils and geomorphology: New York, Oxford University Press, 430 p.
Volcaniclastic sediment of the upper Jackass Mountain Formation (lower to upper Oligocene)—Consists of a lower and an upper unit. The
upper unit is a heterolithic landslide deposit with a white ashy matrix that contains large (1–5 m) angular boulders of porphyritic trachyandesite,
Palisades Tuff, and trachyte breccia. 5–15 m thick. The lower unit is a sandy, matrix-supported, carbonate-cemented conglomerate that contains
upper trachyte lava as the dominate clast. Locally preserved vitric, lithic tuff interbedded with the lower sediment has an 40Ar/39Ar date of 28.23
± 0.06 Ma. 30 m thick.
GODFREY HILLS GROUP
I’’’
Twh
^
Lucas, S.G., 1991, Correlation of Triassic strata of the Colorado Plateau and southern High Plains, New Mexico: New Mexico Bureau of Mines
and Mineral
Resources,
Bulletin 137,
p. 47–56.
The stratigraphy
developed
by Thompson
(1964, 1972) was revised during this project. A full description of the revised stratigraphy is presented
Lucas, S.G.,
2004,
The
Triassic
and
Jurassic
in the report that accompanies this map. systems in New Mexico, in Mack, G.H., and Giles, K.A., eds., The Geology of New Mexico, A Geologic History: New Mexico Geological Society, Special Publication 11, p. 137–152.
Ingram, R.L., 1954, Terminology for the thickness of stratification and parting units in sedimentary rocks: Geological Society of America Bulletin, v.
Tstg
Tsts
65, p. 937-938, table 2.
Twh
Ts
Kc
SIERRA BLANCA VOLCANIC FIELD EXTRUSIVE AND VOLCANICLASTIC ROCKS
1000
?
Feldspathoidal gabbro (essexite) with nepheline (lower Oligocene)—Plug of dark gray to splotchy black and white, feldspathoidal gabbro
Lozinsky, R.P., Hunt, A.P., Wolberg, D.L., and Lucas, S.G., 1984, Late Cretaceous (Lancian) dinosaurs from the McRae Formation, Sierra County,
New Mexico: New Mexico Geology, v. 6, p. 72–77.
Blanca Cenomanian
massif
Hook, S.C., Molenaar, C.M., and Cobban, W.A., 1983, Stratigraphy and revision of nomenclature ofSierra
upper
to Turonian (Upper
Cretaceous) rocks of west–central New Mexico, in Hook, S.C. (compiler), Contributions to mid-Cretaceous paleontology and stratigraphy of New
Mexico – part II: New Mexico Bureau of Mines and Mineral Resources, Circular 185, p. 7–28.
Qa
Tc
Kc
Tim
Kc
Dowe, C.E., McMillan,
N.J., McLemore, V.T., and Hutt, a., 2002, EoceneTwhmagmas Kg
of the Sacramento Mountain,
NM – subduction or rifting?: New
Kc
Tc
K
Ts
Kc
m
lt
d Kt
Mexico Geology,
v. 24, p. 59–60.
Kg
Tc
Kclt
K
Kc
Feldspathoidal gabbro (essexite) with nepheline (lower Oligocene)—Plug of dark gray to splotchy black and white, feldspathoidal gabbro
(essexite; Williams et al., 1954; Moore et al., 1988), Contains large (≤3 cm) phenocrysts of potassium feldspar and plagioclase in an altered,
medium-grained groundmass of nepheline, clinopyroxene, olivine, biotite, and magnetite. Intrudes Walker Group lavas and breccias. Maximum
exposed thickness is 185 m.
exposed thickness is 185 m.
Hook, S.C.,0 2010, Flemingostrea elegans, n. sp.: guide fossil to marine, lower Coniacian (Upper Cretaceous) strata of central New Mexico: New
Mexico Geology, v. 32, no. 2, p. 35–57.
I’’
Godfrey
Peak fault
Tifg
Kues, B.S.,
Lucas,Williams
S.G., Kietzke,
K., and
Mateer,
1985,
Synopsis
Tucumcari
Shale, Mesa
Rica Sandstone,
Pajarito Shale
paleontology,
(essexite;
et al., 1954;
Moore
et al.,N.J.,
1988),
Contains
largeof(≤3
cm) phenocrysts
of potassium
feldspar andand
plagioclase
in an altered,
medium-grained
groundmass
of nepheline,
clinopyroxene,
olivine, biotite,
and Guidebook,
magnetite. Intrudes
Walker Group
lavas and breccias.
Maximum
Cretaceous
of east–central
New Mexico:
New
Mexico Geological
Society
36th Annual
Field Conference,
p. 261–281
3000
Hook, S.C., and Cobban, W.A., 2011, The Late Cretaceous oyster Cameleolopha bellaplicata (Shumard 1860), guide fossil to middle Turonian
strata in New Mexico: New Mexico Geology, v. 33, no. 3, p. 67–96.
3 Rivers
Petroglyph
campground well
(TB-019)
Breccia associated with stocks (lower Oligocene)—Angular to subrounded blocks of fine-grained syenite and Walker Group porphyritic to aphanitic lavas and tuff included within the intrusive rocks near the margins of the stock. The breccia is particularly common in the Rialto stock. Up to 15
Koning,mD.J.,
thick.2009, Radiocarbon age control for Sacramento Mountain-derived alluvial fan deposits near Alamogordo, New Mexico, and related
5000
Broadhead, R., and Jones, G., 2004, Oil, natural gas, and helium potential of the Chupadera Mesa area, Lincoln and Socorro Counties, New
Mexico: New Mexico
I’ Bureau of Geology and Mineral Resources, Open-file Report 478.
Kd
Tsx
Haines, R.A., 1968, The geology of the White Oaks–Patos Mountain area, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University
2000
ofKmdNew
Kt Mexico.
Kclt
Trm
Pag
Py
30000
geomorphic and sedimentologic interpretations [abstract for 2009 NMGS Spring Meeting]: New Mexico Geology, v. 31, no. 2, p. 46.
Birkeland, P.W., 1999, Soils and geomorphology: New York, Oxford University Press, 430 p.
P
Pa
7000
Gillette,
D.D.,
Wolberg, D.L., and Hunt, A.P., 1986, Tyrannosaurus Rex from the McRae Formation (Lancian, Upper Cretaceous), Elephant Butte
Twh
Twh
Ts Sierra
Reservoir,
County, New Mexico: New Mexico Geological Society, Guidebook 37, p. 235–238.
6000
Twh
Ts
Tita
Ps
ag
Kg
Kmd
Kml
Gile,
L.H.,
Peterson, F.F., and Grossman,Kc R.B., 1966, Morphological and geneticPssequences
of KtKdcarbonate
accumulation
in desert soils: Soil
Kd
Kml
Trm
Kmd
PyScience, v. 101, p. 347–360.
Kt
Kd
Pag
Trm
Kml
Kclt
Pa
Twh
Tita
Hook, S.C., Cobban, W.A., 2007, A condensed middle Cenomanian succession in the Dakota Sandstone (upper Cretaceous), Sevilleta National
Wildlife Refuge, Socorro County, New Mexico: New Mexico Geology, vol. 29, no. 3, p. 75–99.
Petroglyph
fault
Kc
Kelley, V.C., 1972, Geology of the Fort Sumner sheet, New Mexico: New Mexico Bureau of Mines and Mineral Resources, Bulletin 98, 55 p.
Kc
Kclt
Psf
Psf
Gile, L.H.,
J.W., and Grossman, R.B., 1981, Soils and geomorphology in the Basin and Range area of Southern New Mexico — Guidebook to the8000
Desert Project: New Mexico Bureau of Mines and Mineral Resources, Memoir 39, 222 p.
Grainger, J.R., 1974, Geology of the White Oaks Mining District, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University of New
4000
Mexico,
Kc 69 p.
100000 geology: Utah Geological and Mineral
120000Survey,
60000 P.W., Machette, M.N., and Haller, K.M.,
80000 1991, Soils as a tool for applied Quaternary
Birkeland,
a division of the Utah Department of Natural Resources, Miscellaneous Publication 91–3, 63 p.
Three Rivers BLM
well (TB-062)
--projecedparallel
to fault
Tist
Tsx
Twh Tist
Ts
Tig
Titb
Kc
Qao
Qao
Qao
Qao
(Thompson, 1973); maximum exposed thickness is 300 m.
9000
Hawley,
Cobban, W.A., 1986, Upper Cretaceous molluscan record from Lincoln County, New Mexico, in Ahlen, J.L., Hanson, ME., and Zidek, J., eds.,
Southwest Three
Section
of AAPG Transactions and Guidebook of 1986 Convention, Ruidoso, New Mexico: New Mexico Bureau of Mines and MinerRivers
Petroglyph
West al
Three
Resources,
p.
77–89.
horst
Rivers
Three Rivers
Runway well
(TB-061)
Lincoln Canyon
Godfrey Pk quad
Nogal Pk quad
Crawford Canyon
Gamble Canyon
TB-150
Winston Canyon
Twh
Fault should be
east-down; it has 40 ft of
SE-down throw
Kc
Ts
Pag
Bonito Canyon
Cross-section D-D’’’’
Tita
Kc
Twh
14 degr app dip based
on att NNW of TB-149;
contact strikes N-S and
to S of well bends to SE
Kt
syeniteGeology
(lower Oligocene)—Initial
intrusive
phase of Rialto
stock;
greenish-gray,
medium-Bureau
to coarse-grained
syenite
containing
plagioclase,
Kelley,
V.C., 1971,
of the Pecos country,
southeastern
New
Mexico:
New Mexico
of Mines and
Mineral
Resources,
Memoir 24,
Tsrs Rialto
75 p Kspar, and sparse anhedral quartz; mafic minerals consist of clinopyroxene, hornblende and biotite. K–Ar date on hornblende is 31.4 ± 1.3 Ma
10000
Cather, S.M., 1991, Stratigraphy and provenance of upper Cretaceous and Paleogene strata of the western Sierra Blanca Basin, New Mexico:
New Mexico Geological Society Guidebook, 42nd Field Conference, p. 265–275.
Py
20000
883 ft min thickness for
Ts using 22 degr attitude
by Candelaria Canyon.
This is consistent with
what is on xsect GG at
JJ intersection
Tc
Kg
Three Rivers quad
Cross-section K-K’
7000
Three Rivers creek
Highway 54
8000
Ts
Kc
11000
9000
Twh
(ft)
Tc
Twtr Tita
Dowe, C.E., McMillan, N.J., McLemore, V.T., and Hutt, a., 2002, Eocene magmas of the Sacramento Mountain, NM – subduction or rifting?: New
Mexico Geology, v. 24, p. 59–60.
diorite having phenocrysts of plagioclase in groundmass of plagioclase, minor Kspar, euhedral biotite, hornblende, and small quartz. Occurs as
Kelley, NE-trending
V.C., and Thompson,
T.B., 1964,
andsyenite
general
of thevolcanic
Ruidoso-Carrizozo
region,
central
Newmaximum
Mexico:exposed
New Mexico
dikes and possible
sills thatTectonics
intrude Rialto
andgeology
Walker Group
rocks. U/Pb date
of 31.8
± 0.5 Ma;
Geological
Society,
Field Conference Guidebook, p. 110–121.
thickness
about 15th
280 m.
Tsrqd
Gile, L.H., 11000
Peterson, F.F., and Grossman, R.B., 1966, Morphological and genetic sequences of carbonate accumulation in desert soils: Soil
Science, v. 101, p. 347–360.
Possible E-down,
NE-striking fault at west
extent of dikes
Kml
absent; quartz sparse, minor arfvedsonite, aegirine, and/or biotite; K–Ar date on biotite is 28.1 ± 1.7 Ma (Moore et al., 1988); preliminary
40
Ar/ 39Ar date on Kspar from west contact in Three Rivers canyon is 28.24 ± 0.19 Ma; maximum exposed thickness is ≥ 850 m.
H’’ Elevation
Tc
Kt
Kgs
Kmd geochemical
Allen, M.S., and TcFoord, E.E.,Tc1991,
Geological,
and isotopic
characteristics
of the LincolnKg County porphyry belt: implications
for
Kml
Kt
Kd
Kt
Kml
Kmd
Kt
Kmd
Trm
Kd
regional tectonics and mineral deposits:
New Mexico
Geological Society
Trm
Kml
Kml Kd
Kd
Pag Guidebook 42, p. 97–113.
Kc
Southwest
10000
Twh
Ts
Tc
Kd
20000
10000
I
f
Trm
REFERENCES
Twtr
2000
Hook,
S.C., Molenaar,
C.M.,
and to
Cobban,
W.A., 1983,
and revision
nomenclature
of upper
Cenomanian light
to Turonian
(lower Stratigraphy
Oligocene)—Highly
variable,of but
voluminous unit
of medium-grained,
gray to (Upper
Rivers quartz
syenite
alkali granite
Tstag Three
1000
bluish-gray,
to porphyritic,
quartz in
syenite
to S.C.
granite;
syenite is Contributions
dominant; contains
Kspar (often large
and distinctlyand
blue–gray)
partly of New
Cretaceous)
rocksequigranular
of west–central
New Mexico,
Hook,
(compiler),
to mid-Cretaceous
paleontology
stratigraphy
most plentiful
at higher
elevations
and
western margin in the unit; plagioclase sparse to
0rimmed
Mexico
– partbyII:other
Newfeldspar;
Mexicoblue–gray
Bureau ofphenocrysts
Mines andare
Mineral
Resources,
Circular
185, p.
7–28.
Kclt
Kg
Bonito Canyon
Py
Psf
Tc
Twtt
Twtr
Kc
4000
ed by
Ingram, R.L., 1954, Terminology for the thickness of stratification and parting units in sedimentary rocks: Geological Society of America Bulletin, v.
65, p. 937-938,
table 2.
Rialto monzonite (lower Oligocene)—Secondary intrusive phase of Rialto stock consisting of white to gray, weakly porphyritic, fine-grained quartz
Intersection of Dry
and Three Rivers
Canyons
Psr
Kc
Twt
t
Tist
Kmd
Three Rivers syenite (lower Oligocene)—Light gray, very coarse-grained syenite consisting primarily of large gray Kspar (anorthoclase) surroundsmall interstial Kspar and quartz, aegirine, arfvedsonite, no apparent plagioclase; a zone of more quartz-rich syenite is found on the east
Cameleolopha
bellaplicata
(Shumard
guideKspar
fossil and
to middle
Hook, margin
S.C., and
Cobban,
W.A., 2011,
The≤10
LatecmCretaceous
of the
unit; sporadically
contains
enclaves of oyster
fine-grained
rock; intruded
by thin porphyritic
dikes1860),
of containing
clinopy-Turonian
3000
strata in
New
Mexico:
New
Mexico
Geology,
v.
33,
no.
3,
p.
67–96.
roxene phenocrysts and unidentified blue and purple minerals (fluorite?); various units not dated; maximum exposed thickness about 650 m.
Tsts
Compton, R.R., 1985, Geology in the field: New York, John Wiley & Sons, Inc., 398 p.
Godfrey Pk quad
Nogal Pk quad
Psr
K
Kc
Km g
lt
d
Km K
t
l
Twtt
Twtt
70000
Kmt
Kg
Kmd
Kmt Hanson,
Ahlen, J.L.,
Kml
Kg
Kml
Kmd New Mexico, in
Kt from Lincoln County,
Cobban,
W.A., 1986, Upper Cretaceous molluscan record
ME., and Zidek, J., eds.,
Kd
Kmt
Kd
Kml
Southwest Section
of
AAPG
Transactions
and
Guidebook
of
1986
Convention,
Ruidoso,
New
Mexico:
New
Mexico
Bureau
of
Mines and 110000
MinerTrm
80000
90000
100000
al Resources, p. 77–89.
Cross-section H-H’’
Py
Psr
Twt
r
Twbpt
60000
Trm
Pag
Kclt
Titd
Psf
Tw
h
Ts
fault
Tgjpt
Tgjt Tgjt Twbpt Tgl
Tgl
Tgl
Kd
Kt
Klm Psf
Kd
Kld
Kg
Kmd
Kd
campground (TB-70;
646 m to the NW)
Psf
Qae
Kg
Godfrey Peak
Tgjb
Kmt
Kg
Tist Three Rivers USFS
Py
Qae
Qae
Jackass Mtn
fault
Jackass
Tgj
ta Mountain
Tgp
Twb
t
Qa
Twt pt
Tgj
d
b
Tgl
Kmd
Kml
Kclt
Kg
Tim
2000
Pag
North Phillips
Hills fault
Kml
Kd
Kt
Kmd
Pag Trm
Kml
Psf
Trm
Pag
Timp
3000
Psf
Trm
50000
Kg
Cross-section D-D’’’’
Alamogordo
fault zone
Phillips Hills
QTbf
TB-200
7000
Highway 54
Jackson Draw
8000
4000
Kclt
Kmd
Cross-section D-D’’’’
Jackson Draw
TB-199
9000
Kc
Kc
H’
10000
5000
Kml
Tr
Pagm
P
P sf
Py sr
40000
11000
6000
Kclt
Km
Wildlife
Refuge, Socorro County, New Mexico: New Mexico Geology, vol. 29, no. 3, p. 75–99.
5000
Tsb
Kc
Cather, S.M., 1991, Stratigraphy and provenance of upper Cretaceous and Paleogene strata of the western
Sierra Blanca Basin, New Mexico:
Kc
Kclt
New Mexico Geological Society Guidebook, 42nd Field Conference, p. 265–275.
Bonito
11000
Blue Canyon
Kc
Kcl
t
H
Tc
Rock House spring
30000
Ts
Kc
Kg
Kt
Kd
Twh
TB-070
K
Km g
d
KmKt
l
r
Tc
Timd
Twh
Twt
Ts
Broadhead, R., and Jones, G., 2004, Oil, natural gas, and helium potential of the Chupadera Mesa area,
Lincoln and Socorro Counties, New Ts
Tc
Tc
Mexico: New Mexico Bureau of Geology and Mineral Resources, Open-file Report 478.
Tc
Ts
Three Rivers Canyon
Ps
Birkeland, P.W., 1999, SoilsTwh
and geomorphology: New York, Oxford University Press, 430 p.
Twh
Tita
Kd
Twh
Ts
Tc
Tc
20000
10000
Twt
t
Twh
Ts
Ts
TB-151
Pa
Py
Pa
Pa
f
Ts
Tc
Twtd
Twtt
Twtt for applied Quaternary geology: Utah Geological and Mineral Survey,
?Soils ?as a ?tool
Birkeland, P.W., Machette, M.N., and Haller,
K.M., 1991,Twtt
a division of the Utah Department
of
Natural
Resources,
Miscellaneous
PublicationTwt91–3, 63 p.
Twtr
Twt
Golondrina Draw quad
Godfrey Pk quad
Ps
Trm
Tc
Twh
Twh
Golondrina Draw quad
Elevation
(ft)
g
Pa
1000
0
Pa
Kc
Twt
r
Twt
t
Qa
TB-66
TB-67
Py
Psf
Py
K
Kc
Km g
lt
d
Km K
t
l
Tgjt
Tgl
TB-68
Psr
Twt
r
Qa
Godfrey Peak
fault
Qa
Lake syenite to syenodiorite (lower Oligocene)—Gray to salt-and-pepper, medium- to coarse-grained syenite in northeast map area;
contains plagioclase, Kspar, minor quartz (≤2%), biotite, hornblende and clinopyroxene (Thompson, 1972; Black, 1978; Constantopoulos, 2007).
Haines,
R.A., 1968,
The body
geology
of the White
Mountain
area,and
Lincoln
Mexico
[M.S.
thesis]:
Albuquerque,
University
10000
Margins
of intrusive
are generally
dioriticOaks–Patos
containing more
plagioclase
maficCounty,
minerals New
than core
syenite;
commonly
contains
aplite dikes
of Newabout
Mexico.
9000 0.1–0.5 m wide. K–Ar date on biotite is 26.6 ± 1.4 Ma (Thompson, 1972); U/Pb date is 27.3 ± 0.04 Ma; maximum exposed thickness
about 425
Rivers
m.alkali granite (lower Oligocene)—Fine- to medium-grained, equigranular to slightly porphyritic, pale gray to salt-and-pepper granite
Tstg Three
8000
elegans,
n. sp.: guideMafic
fossilminerals
to marine,
lower
Coniacian
(Upper Cretaceous)
strata
of central
Hook,
S.C., 2010,
composed
of Flemingostrea
Kspar, quartz, and
minor plagioclase.
consist
of biotite
± arfvedsonite
± aegirine. Some
areas
contain New
sparseMexico:
larger New
Qa
crystals
of
alkali
feldspar.
Some
zones
contain
essentially
no
mafic
minerals.
Rb–Sr
age
(whole
rock)
from
unknown
site
is
26.7
±
1.2
Ma
(Moore
Mexico
Geology, v. 32, no. 2, p. 35–57.
7000
et al., 1991); preliminary 40Ar/ 39Ar date on arfvedsonite from body at top of eastern chair lift, Ski Apache is 27 ± 2 Ma. Maximum exposed
thickness
is ≥ 700
m. 2007, A condensed middle Cenomanian succession in the Dakota Sandstone (upper Cretaceous), Sevilleta National
Hook, 6000
S.C., Cobban,
W.A.,
Tsb
Allen, M.S., and Foord, E.E., 1991, Geological, geochemical and isotopic characteristics of the Lincoln County porphyry belt: implications for
regional tectonics and mineral deposits: New Mexico Geological Society Guidebook 42, p. 97–113.
TB-149
Psr
Psr
Tw
h
Ts
Godfrey Hills
Tgpt
Tgjb
Twbpt
Godfrey Pk quad
Py
Py
Qae
Kg
Qa
Oscura quad
2000
Qae
Timp
Psf
Qae
Psf
Psf
4000
3000
Pag
Phillips Hills
Jackass
Tgj
ta Mountain
Tgp
T
t
Twtwbpt
Tgj
d
b
Tgl
G’’’
G’’
TB-64
fault zone
QTbf
North Phillips
Hills fault
Kml
Kd
Kt
Kmd
Pag Trm
Kml
Psf
Trm
Pag
TB-200
6000 Alamogordo
Highway 54
7000
5000
Jackass Mtn
fault
Jackson Draw
8000
Oscura quad
9000
TB-199
Jackson Draw
10000
Candelaria Canyon
G’
West
11000
Kg
STOCKS
Grainger,
J.R., 1974, Geology of the White Oaks Mining District, Lincoln County, New Mexico [M.S. thesis]: Albuquerque, University of New
Elevation
Mexico,
69
(ft) p.
East
REFERENCES
Godfrey Pk quad
G
Kclt
Kmd
Kt
Kml
Gillette,minerals
D.D., Wolberg,
D.L., and
Hunt,0.1–0.5
A.P., 1986,
RexBlanca,
from the
Formation
(Lancian,
Upper
Cretaceous),
Elephant Butte
and plagioclase
(mostly
mm inTyrannosaurus
size). Near Sierra
theMcRae
groundmass
contains
hornblende
± biotite
and xenolithos
of pink,
coarse-grained
may
be present.
rock commonly
develops a strong
very strong varnish.
Reservoir,
Sierra
County, Newsyenite
Mexico:
New
MexicoExposed
Geological
Society, Guidebook
37, p.to235–238.
Elevation
(ft)
Breccia associated with stocks (lower Oligocene)—Angular to subrounded blocks of fine-grained syenite and Walker Group porphyritic to aphanitic lavas and tuff included within the intrusive rocks near the margins of the stock. The breccia is particularly common in the Rialto stock. Up to 15
m thick.
Muds one and sha e oodp a n depos s dom na e n he owe 280–300 m o h s un F oodp a n depos s cons s o g ay o da k g ay o g een
sh g ay ss e o b ocky sha e and muds one Es ma e 1–5% coa beds o o gan c ch muds one beds ha a e gene a y ess han 1 m h ck Loca
y on ox de s de e? conc e ons a e p esen Sands one channe s a e 1–5 m h ck and pa e ye ow o ye ow Basa con ac s d awn a he
uppe mos she bea ng bed o un Kc To a h ckness 550 m
Trachybasalt
Eocene)—Gray
to dark
gray, aphaneticand
to sparsely
porphyritic
dikes. Locally,
these dikesinare
spotted.
2000
Titb L.H.,
Gile,
Peterson,intrusions
F.F., and(upper
Grossman,
R.B., 1966,
Morphological
genetic finely
sequences
of carbonate
accumulation
desert
soils: Soil
Phenocrysts, where present, consist of plagioclase. Groundmass is composed of plagioclase, olivine, clinopyroxene ± phlogopite.
Science, v. 101, p. 347–360. 1000
Kclt
Kg
Kmd
Kt
Kml
180000
Kc
Cather, S.M., 1991, Stratigraphy and provenance of upper Cretaceous and Paleogene strata of the western Sierra Blanca Basin, New Mexico:
10000
Dikes and
other intrusions
withGuidebook,
megacrystic,42nd
aligned
plagioclase
(upper
Eocene)—A distinctive, light gray to dark gray intrusive rock containing
New
Geological
Society
Field
Conference,
p. 265–275.
Timp Mexico
Kcu
Kg
Pag
F’’’’
Tsrs
Tc
Kcu
Kcl
Kclt
Tsrs
Ts
Kcu
Kclt
Twt
Variably non-porphyritic to porphyritic. Phenocrysts are composed of potassium feldspar, plagioclase, and biotite. Locally, hornblende and quartz
phenocrysts are observed. Equigranular varieties are common in the northwest part of the compilation map, west of Cub Mountain, where grains
Broadhead,
R., and
G., 2004,
Oil, natural
gas, and and
helium
potential
of the Chupadera
Mesa
area,
and Unit
Socorro
Counties, New
are 0.5–2.0
mm,Jones,
subhedral,
and composed
of plagioclase
potassium
feldspar(?),
with about 25%
biotite
andLincoln
hornblende.
also assigned
Elevation
Mexico:
New
Mexico
Bureau
of
Geology
and
Mineral
Resources,
Open-file
Report
478.
to a prominent, ENE orientated dike south of the Three Rivers drainage, containing phenocrysts of feldspar, pyroxene, and subordinate biotite; the
(ft)
groundmass
is aphanitic. 11000
Northeast
Twh
Twh
Kcu
Kcl
Kcu
Ts
Ts
Tc
Twtt
Tist
Tc
Twh
Twtd
Twtat
Twtt
Twtr
Twtr
Ts
Tc
Ts
Twt
Qa
Qa
Qa
Twbpt
Twtt
Twtr
Ts
Tc
Pag
Psr
Tnt
Twtat
dikes (upper Eocene to lower Oligocene)—Light gray to light grayish-white to light reddish-gray to tan, biotite-bearing intrusions.
Titd Trachydacite
Birkeland,
P.W., 1999,
Soils and geomorphology: New York, Oxford University Press, 430 p.
Cross-section C-C’’’’
Cross-section D-D’’’’
Tim
Kclt
Kmd
Kd
Pa
Twtt
Twtr
Twtt
Twh
Twh
Twh
Py
Pa
Qa
TB-135
6000
TB-112
TB-111
7000
TB-128
8000
TB-127
Phillips springs
9000
TB-115
TB-114
TB-116
10000
TB-132
TB-125 & 126 (660 m to S)
Milagro springs
TB-130 (536 m to S)
TB-178
TB-181
TB-133
TB-180
TB-179
Southwest
TB-131
F
11000
Rialto syenite (lower Oligocene)—Initial intrusive phase of Rialto stock; greenish-gray, medium- to coarse-grained syenite containing plagioclase,
Kspar, and sparse anhedral quartz; mafic minerals consist of clinopyroxene, hornblende and biotite. K–Ar date on hornblende is 31.4 ± 1.3 Ma
(Thompson, 1973); maximum exposed thickness is 300 m.
SED MENTARY ROCKS THAT PRE DATE THE S ERRA BLANCA VOLCAN C F ELD
long. Locally, phenocrysts include hornblende and/or pyroxene. Groundmass feldspar probably includes albite, microline, and orthoclase. These
feldspar
are commonly
long, platy
stacked,
foliated
texture.
1–25% mafic
minerals
0.1–0.5
mm long,and
which
locally Survey,
Birkeland,
P.W.,grains
Machette,
M.N., <1
andmm
Haller,
K.M.,and
1991,
Soilsproducing
as a tool afor
applied
Quaternary
geology:
Utah
Geological
Mineral
include
biotite
and
pyroxene
±
amphibole.
Up
to
1%
quartz
and
1–5%
possible
sanidine.
a division of the Utah Department of Natural Resources, Miscellaneous Publication 91–3, 63 p.
Elevation
(ft)
Rialto monzonite (lower Oligocene)—Secondary intrusive phase of Rialto stock consisting of white to gray, weakly porphyritic, fine-grained quartz
diorite having phenocrysts of plagioclase in groundmass of plagioclase, minor Kspar, euhedral biotite, hornblende, and small quartz. Occurs as
NE-trending dikes and possible sills that intrude Rialto syenite and Walker Group volcanic rocks. U/Pb date of 31.8 ± 0.5 Ma; maximum exposed
thickness about 280 m.
Psf
4000
Kt Kmd
4000
Kd Kml
Kcl
Kcu
Alkali
diorite
and
syenodiorite
(Eocene
to
lower
Oligocene)—Equigranular,
fine- to medium-grained, salt-and-pepper textured dikes and sills with
Trm
Tid
3000
Pag
Kcuvariable plagioclase feldspar and pyroxene
Kg
Kcl
phenocrysts.
These
intrusive
bodies
may grade into more porphyritic textures (Tita). Alkali diorite may
Psf
Kcu
Kmd
Kclt et al., 1988). Psr
contain amphibole and biotite (Moore
2000
Kg
Kml
REFERENCES Kclt
Kcl
Trm Py
Kt Kmd
1000
Pag
Kd Kml
Syenite and trachyteKg
(upper Eocene
and Psf
lower
to upper Oligocene)—This inclusive unit is applied to light-colored, intrusive rocks dominated by
Tist
Kmd
Trm
Kt Allen, M.S., Kt
Psr geochemical
and Foord,
E.E., 1991,
Geological,
isotopic
characteristics
of thetan
Lincoln
County
belt:
implications
plagioclase
and potassium
feldspar.
Unit occurs
as stocks, sills, and
and dikes.
ranges from creamy
to creamy
whiteporphyry
to light pink
to light
gray
Pag
0 Color
Kml
Kcu
Kcl
Kml
Kd
TRm
Pag
Intrusion of brecciated, porphyritic trachyte of the Jackass Mountain Formation (lower Oligocene)—Similar to unit Tgjb but in sills, dikes, or
Elevation
small plugs.
(ft)
East
11000
Monzonite to diorite (Oligocene?)—Light gray to gray to greenish-gray, weathering tan to brown, aphanetic to medium-grained (less commonly,
10000
coarse-grained) phaneritic igneous rocks forming dikes, sills, and irregular
intrusive masses. Composed of feldspar and mafic minerals, but sparse
quartz may be present north of Nogal. Feldspar consists of varying proportions
9000 of plagioclase and lesser potassium feldspar. Mafic minerals may
include pyroxene, amphibole and biotite.
Tc
Tc
Kcu
Qa Kth
Kth
Rhyolite to granite (Oligocene)—White to pale orange, aphanitic and typically aphyric, igneous rocks forming dikes, sills, and irregular igneous
masses north of Nogal. Where present, phenocrysts consist of <10% quartz. Unit includes intrusion of Vera Cruz Mountain of Rawling (2011). This
intrusion exhibits a core of biotite-phyric granite or syenite surrounded by aphyric trachyte and quartz-phyric trachyte. Commonly associated with
faults.
Ts
Tc
Tim
Tid
Py
Psr
Pa
Tirt
Twtr
Twhf
Tim
Kmd
Psr
TB-240
Qa
Twtr
Twhf
Ts
Tc
Kg
Kmd
180000
Twtas
Twtas
Twhs
Kcu
Kcu
Kclt Kcl
Kg
Kclt
Pag
Kth
Intrusive rocks, undivided (Eocene to Oligocene)
Tirg
Twtr
Tc
Tc
Kcu
Twhs
Twtas
Qa Kg
Kg
Kmd
Py
Ts
Ts
140000
120000
Twhf
Kth
Py
110,000 ft
Ts
Kclt
Kg
Psr Psf
Py
Pa
Twh Twh
s
f
Kcu
Kd
Trm
Py
Twtd
Twtr
Twt
Twh Twh r
s
f
Psr
Py
E’’’
Twh Twhf
s
Kmd
Kclt
SIERRA BLANCA AND CAPITAN INTRUSIVE ROCKS
Psr
100,000 ft
Qa
Twtas
Twtr
Kml
Kd
TRm
Psf
Ti
Twtd
Twtas
Twtas
Twtr Twtr
Twh
Kmd
Kd
TRm
Psr
Pa
Qa
Kml
Pag
Py
90000 ft
unconfined flow in basal QTbf
confined flow
Twbpt
Basalt of the Malpais (middle Holocene)—Gray, vesicular basalt that contains 5% phenocrysts of pyroxene (0.5–2.0 mm long). Groundmass is
3000
0.1–0.3 mm and a mix of plagioclase and pyroxene(?). Up to several meters thick.
Psf
Py
Kc
Kg
Pag
Psr
Psr
Qbm
Kth
TRm
Kd
Pag
Psf
Py
Psf
Kml
Kmd
Kth
Kmd
Kmd
Pag
Psr
Pag
Kg
Kg
Kg
Kc
Kclt
Tid
Qa
Kc
Kclt
Kg
Kclt
Kg
Kmd
Psf
TRm
Py
Kmd
Kth
Kml
Kc
Kc
Tita
Qa
Titd
Tc?
Kclt
Kclt
Kclt
Pag
Kml
Pag
Kclt
Kg
Kmd
Pag
Pag
70000 ft
Kth
Kmd
Kml
TRm
Kclt
Kg
Kclt
Kth
Kmd Kth
Golondrina
Draw quad
Cross-section H-H’’
Godfrey
Peak quad
Cross-section G-G’’’
Candelaria Canyon
Godfrey Peak
Cross-section F-F’’’’’
Kcc
Kclt
Py
Pa
60000
Kcc
Qa
Tc
Kcu
Kclt
Psf
Kclt
Kg
Kg
Qa
Kg
Kmd
Kml
Tita
Kclt
Tim
QUATERNARY
Kcc
Qa
Qa
Qa
Qa
Kcc
Kclt
Kclt
TRm
Kclt
E’’
Py
Pag
Kclt
Kcl
Kc
Kcc
Kml
Kcc
Kclt
Kg
Kclt
Kg
Kclt
Kg
Twt
D’’’
IGNEOUS AND VOLCANICLASTIC ROCKS
Qa
Titb Tcm
Kcc
Kcc
Kcc
Kmd Kth
Kcc
Tcm
Tcm
Tcm
Laramide
deformation
Kg
Kcc
Kcc
Titb
Tigjb
Tita
Pag
Psr
Kml
Trm
Pa
Pb+IPh+IPb
10000
Kclt
Kg
Kmd
Kt
Kc
Kclt
Kcl
Tita
Kc
Tita
Tita
Kcu
Psr
Pa
Pb+IPh+IPb
Pb+IPh+IPb
0
Psr
Py
Py
Pa
Pag
Psf
Psr
Py
undivided
Mesozoic
and
Paleozoic
rocks
2000
Psf
Kml
Kd
Trm
Pag
Psf
Pag
Kmd
Kt
Kclt
Tsc
Qa
Titb
Kcc
Kcc
Tcm
Kclt
Kcc
Titb
TB-236
7000
Jakes Hill
8000
Highway 54
Root spring
Cottonwood Creek
9000
Three Rivers quartz syenite to alkali granite (lower Oligocene)—Highly variable, but voluminous unit of medium-grained, light gray to
bluish-gray, equigranular to porphyritic, quartz syenite to granite; syenite is dominant; contains Kspar (often large and distinctly blue–gray) partly
rimmed by other feldspar; blue–gray phenocrysts are most plentiful at higher elevations and western margin in the unit; plagioclase sparse to
absent; quartz sparse, minor arfvedsonite, aegirine, and/or biotite; K–Ar date on biotite is 28.1 ± 1.7 Ma (Moore et al., 1988); preliminary
40
Ar/ 39Ar date on Kspar from west contact in Three Rivers canyon is 28.24 ± 0.19 Ma; maximum exposed thickness is ≥ 850 m.
WALKER GROUP
Older basin fill of the Tularosa Basin, undivided (Miocene to lower Pliocene?)—Clayey-silty, very fine- to medium-grained sand interbedded
with minor conglomerate beds, locally with minor scattered medium- to very coarse-grained sand and 1–10% pebbles. Mapped south of the Three
Rivers drainage on the footwall of the Alamogordo fault. Unconformably lies beneath unit Qao1, and is distinguished from younger deposits by
smaller gravel sizes, common calcium carbonate-impregnation of gravel beds, strong consolidation, and steeper dips. Base is not exposed. Colors
of non-gravelly beds range from very pale brown to light yellowish-brown to light brown to pink. Paleosols are characterized by
calcic horizons
Elevation
(Stage II morphology in limited exposures) underlain by gypsic horizons; locally, the calcic horizons are overlain by thin, yellowish-red,
illuviated
(ft)
clay horizons. Greatest exposed thickness is 2 m, but unit is 120 m thick at the Lewelling #1 well (see cross section). On the immediate
fault hanging
8000
wall, basin-fill is up to ~700 m thick (see cross section).
Tbf
Church Mtn quad
Nogal quad
Bull Gap quad
10000
Cub Mtn quad
E’
West
3000
50000 ft
Tsc
Tsc
Kcc
Tcm
Qa
Titb
Titb
Tcm
Laramide
deformation
Tcm
Tcm
Tcp
Three Rivers
cross-section
Tcm
Tsc
Twh
Tcm
Kcu
Kg
Kmd
Kg
Kml
Kmd
Trm
Pag 60000 ft
Tita
Tsc
Twtr
Tcm
D’’’
Qa
Th
Tis
Tsc
Tsc
Tcm
Kcl
Tsc
Twh
Twh
Qa
Tis
Tsc
Twtr
Twtr
Twh
Twtt
Tsc
Tsc
Kcu
Kt
Twtt
Twbpt
Twtt
Twh
Twbpt
Twtt
Tis
Twh
Twh
Tnpt
7000
TB-222
E
Twh
TB-188
40000 ft
Tc
TB-189
30000 ft
Cross-section D-D’’’’
20000 ft
Twtr Twtt
Twtr
Twh
Tcm
?
10000 ft
Twtr
Ts
Tc
Kcu
Py
0
Godfrey
Peak quad
Cub Mtn
quad
Kcl
Twh
Twh
Ts
Twbpt
Tgl
Twbpt
H - H’
Cross-section CC
Pag
Py
1000
Elevation
(ft)
11000
Chavez Draw
Kd
Ps
Pg
Py
Py
Kclt
Kg
Kmd
Kml
Trm
Pag
Ps
Twtt
Tgl
Tgjpt
Tgl
Tis
Tgjpt
Tgjta
Titb
Kml
Trm
Ps
Pg
2000
Kmd
Kt
Kml
TR
Kclt
Kg
Tc
Tgjb
Tgjpt
Qa
Timp
Kg
Kmd
Ts
Qa
Tgl Tgjb Tgjta Twbpt
Qa
Tita
Kt
Kd
Tist
Tgjb
Tgjtd
G - G’
Cub Mtn quad
Church Mtn quad
Kml
TR
Pag
Ps
Pg
Py
3000
Kd
TR
Kcl
Tita
F - F’
Rattlesnake Spring
4000
Qa
Pag
Ps
Tita Tist
Jakes
fault
Qa
North
TB-190
(screened
in Qa to N)
5000
Qa
?
Malpais
Qbm
?
6000
Willow Draw
7000
Highway 54
Harkley Draw
North
8000
Rim Rock Canyon
Elevation
(ft)
Cottonwood Creek
D
Cross-section E-E’’’’
Carrizozo
West quad
Cub Mtn
quad
D’’
Tkgf
High-level sandy gravels (Pliocene to lower Pleistocene)—Sandy gravel whose base is >15 m above present drainage bottoms and above straths
associated with Qao1. Unit not exposed, but surface gravel consist of pebbles and cobbles with 1–10% boulders. Where present, an eroded
horizon of relatively large clasts is used to map the base of this terrace deposit. 1–10 m-thick.
QTg
D’
Tgl
Older allostratigraphic subunit of older alluvium (lower to middle Pleistocene)—Sandy gravel under topographic highs, locally overlying
exposed bedrock, that grades westward into intercalated sandy pebbles, pebbly sand, sand, and clayey-silty sand. Finer-grained sediment
appears to dominate progressively south of the Three Rivers drainage. Unit lacks the buried soils that are commonly observed in Qao2, typically
contains coarser gravels, and is locally very gypsiferous. The unit contains a basal sandy gravel, 1–3 m thick and commonly strongly cemented,
which is overlain by a coarsening-upward sequence. Sandy gravel is dominated by stream-flow facies, with lesser amounts of debris-flow facies.
Gravel is mostly clast-supported, locally imbricated, and consists of pebbles with subequal to subordinate cobbles and boulders. About 1–3% of
clasts disintegrate readily. Sand is mostly medium- to very coarse-grained. Debris flow sediment contains abundant cobbles and boulders that are
commonly matrix-supported. Fine-grained sediment ranges from reddish to very pale brown. Clay, silt, and very fine- to fine-grained sand become
increasingly common away from the mountain front. Sand in fine-grained deposits is mostly very fine- to fine-grained, with subordinate medium to
very coarse grains that are commonly scattered. Base of deposit is typically >6 meters above the base of unit Qao2. In the south, a prevalent petrogypsic horizon developed on its surface with very strongly varnished surface clasts. In the north, top soil is characterized by strong calcium carbonate + gypsum accumulations (Stage III to IV calcium carbonate morphology). Weakly to moderately consolidated. 1–35 m thick.
2000
Kclt
80000
Tgjt
Base of unit lies several meters below the base of unit Qao1, and its surface contains strong gypsum or calcic/gypsic horizon(s) with Stage III-IV
apparent carbonate morphology. Strong clast varnish and a well-developed desert pavement where unit is not covered by slopewash or sheetflood deposits (Qse). Several non-differentiated erosion surfaces. Weakly to well consolidated, non-cemented. Unit grades downward into Santa
Fe Group deposits west of the Alamogordo fault. Exposures are 3–15 m thick.
8000
Ts
Kg
Kg
Kmd
Twh
Tc
Kcl
Kg
Kmd
9000
Twt
Twt
Kcu
Tgjpt
In coarse channel fills, gravel is dominated by pebbles but cobbles and boulders are abundant close to the mountain front. Gravel is commonly
clast-supported and imbricated, but cobbly, massive debris flow beds locally fill paleochannels. Sand is mostly medium- to very coarse-grained.
10000
Tc
Kcu
Kcu
Tgjb
Middle allostratigraphic subunit of older alluvium (middle to upper Pleistocene)—The extensive Qao2 probably represents multiple aggradational events that were amalgamated into seemingly one deposit. Unit consists of interbedded fine-grained sediment and sandy gravel and pebbly
sand, and locally exhibits a coarsening-upward trend (where the upper part consists of amalgamated or stacked channel-fills). Finer sediment
consists of gypsiferous, reddish to very pale brown, very fine- to medium sand and clayey fine sand, with minor coarse- to very coarse-grained sand
and pebbles (scattered or in very thin to medium lenses). Buried soils commonly have a relatively thin, slightly reddened horizon (locally with illuviated clay) underlain by a calcic horizon (Stage I to II carbonate morphology) underlain by a gypsic horizon. Locally, rhizoliths are present that are
cemented by gypsum.
Elevation
(ft)
11000
Southeast
Ts
Tc
Kcu
Twtt
C’’’’
C’’’
Ts
Tc
Kg
Kmd
Kml
Twtd
Twh
Ts
Ts
Tc
TRm
Pag
Twtr
Twh
Twtr
Twh
Kth
Py
10000
Twtat
Kc
Kg
Ps
1000
Twtat
Twtt
Twtr
Twtt
Tc
Kml
TR
Pg
0
Twtt
Twtr
Ts
Kcl
Kmd
Twtd
Twtd
Qa
Kcu
Kml
Kd
Pag
Ps
Pg
Kmd
Qa
TB-218
6000
Tkgf
Twbpt
Wells 218, 220, and 21 are near
the Carrizozo city well field
TB-177
TB-176
TB-113
TB-173
7000
TB-118
Anchor Spring
9000
TB-186
TB-220
TB-221
10000
8000
Cub Mtn quad
Church Mtn quad
11000
C’’
C’
Northwest
Carrizozo W quad
Cub Mtn quad
C
Tgjbt
On the surface, clast varnishing is relatively strong, and there is a well-developed desert pavement where unit is not covered by slopewash or sheetflood deposits (Qse). A strong gypsum horizon (comparable to a Stage III calcium carbonate morphology) is developed on top of this unit to the
south, with strong Stage III to IV calcic horizons more common to the north. Locally, a reddish-yellow Bw or Bt soil horizon overlies calcic horizons.
In places, such as along Willow Draw and Harkey Draw, surface erosion has resulted in a general lack of a notable calcic horizon. Weakly to
well consolidated. 3–12 m-thick.
1000
Py
Pag
70000
2000
Qao2
Elevation
(ft)
Tgjta
Finer-grained sediment is light brown (7.5 YR 6/4) to reddish-yellow (7.5 YR 6/6) to reddish-brown (5 YR 5/4), hard, gypsiferous, and composed
of silty-clayey very-fine to fine-grained sand (locally with medium to very coarse sand) in thin to thick, tabular beds (also internally massive). Within
the floodplain sediment are 20–25% interbeds of fine- to very coarse-grained sand and sandy pebbles; these coarse beds are very thin to thin and
lenticular to tabular. There may also be up to 5–15% scattered pebbles and up to 15% scattered medium- to very coarse-grained volcanic sand.
The tread of this unit lies as much as 6 m below adjacent Qao2 surfaces.
5000
Kg
Kc
Kt
40000
Tgjvs
Younger allostratigraphic subunit of older alluvium (upper Pleistocene)—Sand and gravel inset into the middle subunit of older alluvium (Qao2),
locally occupying paleo-valleys. Contains interfingering coarse channel-fills and finer-grained deposits that locally exhibit a coarsening-upward
trend. Gravel is clast-supported, locally imbricated, gypsiferous (but seemingly less gypsum than in units Qao2 and Qao1), and consists of very
fine to very coarse pebbles with subordinate to subequal cobbles and 1–25% boulders. Debris flow sediment is locally observed (<10% of
sediment volume away from bedrock highs) and commonly has matrix-supported cobbles. Sand is mostly medium- to very coarse-grained. Coarse
beds are weakly to moderately consolidated and non-cemented. Thick clay colloids commonly coat sand grains and clasts.
Qao3
10000
Ts
Py
30000
TB-36Church Mountain quad
TB-35 Nogal quad
TB-41
TB-171
Qa
(ft)
11000
Southeast
Tc
Kd
TRm
Three Rivers syenite (lower Oligocene)—Light gray, very coarse-grained syenite consisting primarily of large gray Kspar (anorthoclase) surrounded by small interstial Kspar and quartz, aegirine, arfvedsonite, no apparent plagioclase; a zone of more quartz-rich syenite is found on the east
margin of the unit; sporadically contains ≤10 cm enclaves of fine-grained rock; intruded by thin porphyritic dikes of containing Kspar and clinopyroxene phenocrysts and unidentified blue and purple minerals (fluorite?); various units not dated; maximum exposed thickness about 650 m.
The stratigraphy developed by Thompson (1964, 1972) was revised during this project. A full description of the revised stratigraphy is presented
in the report that accompanies this map.
Older alluvium, undivided (Pleistocene)—Undifferentiated older alluvium recognized by its red hues, abundant gypsum, and locally well-developed, buried soils. To the south, rhizoliths commonly seen that are cemented by gypsum. There are varying proportions of gravelly channel-fills, in which gravel content decreases and sand content increases in a downstream direction; gravel dominates within 1–2 km of mountain
fronts. Gravel consists of pebbles, cobbles, and minor boulders. Top soil characterized by a reddish Bw or Bt horizon (where preserved), underlain
by horizons of Stage III to IV calcium carbonate and/or gypsum accumulation, with gypsum content increasing to the south. Base of unit generally
not exposed. Unit is commonly overlain by younger, finer-grained sheetflood deposits, correlative to Qse. Well consolidated and up to 25 m thick.
B’’’’ Elevation
B’’’
Kc
Kclt
Kmd
2000
Carrizozo East quad
Tc
Kc
Kg
TB-216
TB-217
TB-124
Qa
MW-11
Qbm
TB-120
TB-119
6000
TB-23
Qbm to
west
7000
TB-215
8000
Scott Spring
TB-101
TB-100
TB-102 & 103
9000
Bonito Lake syenite to syenodiorite (lower Oligocene)—Gray to salt-and-pepper, medium- to coarse-grained syenite in northeast map area;
contains plagioclase, Kspar, minor quartz (≤2%), biotite, hornblende and clinopyroxene (Thompson, 1972; Black, 1978; Constantopoulos, 2007).
Margins of intrusive body are generally dioritic containing more plagioclase and mafic minerals than core syenite; commonly contains aplite dikes
about 0.1–0.5 m wide. K–Ar date on biotite is 26.6 ± 1.4 Ma (Thompson, 1972); U/Pb date is 27.3 ± 0.04 Ma; maximum exposed thickness
about 425
Three
Rivers
m.alkali granite (lower Oligocene)—Fine- to medium-grained, equigranular to slightly porphyritic, pale gray to salt-and-pepper granite
composed of Kspar, quartz, and minor plagioclase. Mafic minerals consist of biotite ± arfvedsonite ± aegirine. Some areas contain sparse larger
crystals of alkali feldspar. Some zones contain essentially no mafic minerals. Rb–Sr age (whole rock) from unknown site is 26.7 ± 1.2 Ma (Moore
et al., 1991); preliminary 40Ar/ 39Ar date on arfvedsonite from body at top of eastern chair lift, Ski Apache is 27 ± 2 Ma. Maximum exposed
thickness is ≥ 700 m.
SIERRA BLANCA VOLCANIC FIELD EXTRUSIVE AND VOLCANICLASTIC ROCKS
Terrace gravel, undivided (Pleistocene)—Undifferentiated terrace deposits flanking major drainages. Composed primarily of sandy
pebbles–cobbles and lesser boulders. Straths located 3 to 15 m above local base level. In the southwest compilation map area, this unit was
applied to thin(?), highly gypsiferous deposits overlying erosional surfaces greater than 10 m above active drainages. Generally 0.5–2.0 m thick,
but locally as thick as 5 m.
Qtg
B’’
Carrizozo West quad
Carrizozo East quad
10000
Tifg
Intermediate alluvium (uppermost Pleistocene)—Unit locally seen in arroyo cuts disconformably between units Qao below and Qay1 above.
Sediment consists of reddish-brown, commonly clay-rich, very fine- to very coarse-grained sand and pebbly sand that is massive; pebbles occur
as isolated, matrix-supported clasts and in thin, discontinuous lenses. Larger dimension gravel beds are laterally continuous, well-bedded, and
clast-supported but matrix-rich; these may contain up to 10% cobbles. Locally contains gypsum rhizoliths or filaments. Topsoil marked by common,
macroscopic clay illuviation textures, rare disintegrating clasts, and Stage I+ to II+ carbonate morphology underlain by Stage I gypsum accumulation. Weakly to well consolidated 1–3(?) m thick.
Qai
0
50000
B’
Northwest
11000
Megacrystic, alkali gabbro–diorite or syenogabbro–diorite intrusions (middle? to upper Eocene)—Dark gray to gray to greenish-gray,
porphyritic hypabyssal rocks occupying sills, dikes, and laccoliths. Groundmass is 0.2–0.5 mm, less commonly to 1.0 mm, and consists of
plagioclase with 15–25% pyroxene and local hornblende. Rock has 2–25% phenocrysts composed of hornblende ± pyroxene (up to
20–60 mm long) and 5–20% smaller plagioclase. Groundmass consists of plagioclase with subordinate, but variable, amounts of mafic
minerals and plagioclase (mostly 0.1–0.5 mm in size). Near Sierra Blanca, the groundmass contains hornblende ± biotite and xenolithos
of pink, coarse-grained syenite may be present. Exposed rock commonly develops a strong to very strong varnish.
Younger alluvium overlying intermediate alluvium—Generally mapped in the west–east valley north of the Godfrey Hills. See descriptions for
units Qay and Qai.
1000
TB-38 Church Mountain quad
B
Trachybasalt intrusions (upper Eocene)—Gray to dark gray, aphanetic to sparsely finely porphyritic dikes. Locally, these dikes are spotted.
Phenocrysts, where present, consist of plagioclase. Groundmass is composed of plagioclase, olivine, clinopyroxene ± phlogopite.
Qay/Qai
Qao
Elevation
(ft)
Trachyandesite intrusions, including minor trachybasalt (upper Eocene)—Porphyritic intrusive rocks that are common throughout the map area,
commonly occurring as dikes or sills. These rocks are typically light gray to dark gray, locally weathering to reddish-brown to brownish-gray.
Exposed rocks generally do not develop as strong a varnish as that on Tim. Up to 35% phenocrysts of pyroxene (0.5–10 mm-long) and feldspar
(probably plagioclase, 0.5–11 mm long); locally, hornblende phenocrysts are observed. Feldspars are commonly aligned. Groundmass is
composed of feldspar that ranges from 0.1–0.5 mm together with 10–35% pyroxene(?) ± biotite (0.1–0.5 mm long).
2000
Py
30000
Dikes and other intrusions with megacrystic, aligned plagioclase (upper Eocene)—A distinctive, light gray to dark gray intrusive rock containing
about 15–20% large phenocrysts (0.1–2.0 cm long) of tabular plagioclase in an equigranular to fine-grained matrix of plagioclase and pyroxene
(0.1–0.5, mostly 0.1–0.3 mm). The plagioclase laths are often distinctively aligned parallel to the margins of the dikes. Probable intrusive equivalent
of megacrystic plagioclase-bearing lavas in the Rattlesnake Member of the Three Rivers Formation, which is the basis of the upper Eocene age
interpretation.
This unit appears to overlie an unconformity developed at about the stratigraphic level of the Bucky Pasture Tuff. Includes the 28.2 to 28.8 Ma
Jackass Mountain Formation and the 28.8 to 34.3 Ma Lopez Spring Formation.
3000
Py
1000
Trachydacite dikes (upper Eocene to lower Oligocene)—Light gray to light grayish-white to light reddish-gray to tan, biotite-bearing intrusions.
Variably non-porphyritic to porphyritic. Phenocrysts are composed of potassium feldspar, plagioclase, and biotite. Locally, hornblende and quartz
phenocrysts are observed. Equigranular varieties are common in the northwest part of the compilation map, west of Cub Mountain, where grains
are 0.5–2.0 mm, subhedral, and composed of plagioclase and potassium feldspar(?), with about 25% biotite and hornblende. Unit also assigned
to a prominent, ENE orientated dike south of the Three Rivers drainage, containing phenocrysts of feldspar, pyroxene, and subordinate biotite; the
groundmass is aphanitic.
Younger alluvium, with subordinate recent alluvium (Holocene)—See descriptions for units Qay and Qar. Mapped near modern drainages
where Qay and Qar could not be differentiated at this map scale.
4000
Pg
Syenite and trachyte (upper Eocene and lower to upper Oligocene)—This inclusive unit is applied to light-colored, intrusive rocks dominated by
plagioclase and potassium feldspar. Unit occurs as stocks, sills, and dikes. Color ranges from creamy tan to creamy white to light pink to light gray
to gray. Stocks and many other intrusions are commonly porphyritic, with phenocrysts composed of orthoclase and plagioclase that are 1–20 mm
long. Locally, phenocrysts include hornblende and/or pyroxene. Groundmass feldspar probably includes albite, microline, and orthoclase. These
feldspar grains are commonly <1 mm long, platy and stacked, producing a foliated texture. 1–25% mafic minerals 0.1–0.5 mm long, which locally
include biotite and pyroxene ± amphibole. Up to 1% quartz and 1–5% possible sanidine.
Qayr
6000
Kd
Alkali diorite and syenodiorite (Eocene to lower Oligocene)—Equigranular, fine- to medium-grained, salt-and-pepper textured dikes and sills with
variable plagioclase feldspar and pyroxene phenocrysts. These intrusive bodies may grade into more porphyritic textures (Tita). Alkali diorite may
contain amphibole and biotite (Moore et al., 1988).
GODFREY HILLS GROUP
http://geoinfo.nmt.edu/publications/maps/geologic/ofgm/home.html
7000
TR
Pag
Rhyolite to trachyte (Oligocene)—White to gray, aphyric to porphyritic, felsic intrusions interpreted to be of rhyolite or trachyte composition.
Intrusions consist of dikes and small plugs associated with the Three Rivers stock. Phenocrysts include Kspar, quartz, biotite, and plagioclase.
Locally, flows of aphyric rhyolite are included in this unit; these are typically flow-banded and folded and contain microphenocrysts of
quartz). are included in this unit (i.e., Oak Grove rhyolite of Goff et al., 2011). Unit also includes fine- to coarse-grained, pale pink to pale
tan dikes containing Kspar, quartz, minor plagioclase, minor biotite, and arfvedsonite (these cut the Walker Group and various syenite units).
This and other STATEMAP quadrangles are (or soon will be) available
for free download in both PDF and ArcGIS formats at:
8000
Tist
Monzonite to diorite (Oligocene?)—Light gray to gray to greenish-gray, weathering tan to brown, aphanetic to medium-grained (less commonly,
coarse-grained) phaneritic igneous rocks forming dikes, sills, and irregular intrusive masses. Composed of feldspar and mafic minerals, but sparse
quartz may be present north of Nogal. Feldspar consists of varying proportions of plagioclase and lesser potassium feldspar. Mafic minerals may
include pyroxene, amphibole and biotite.
The youngest allostratigraphic unit back-fills narrow paleovalleys cut in the second-oldest unit, and consists of pale brown to very pale brown to
light brownish-gray, well-stratified sand with minor beds of pebbles. The top soil of the youngest allostratigraphic unit is marked by slight calcium
and gypsum accumulation (comparable to a Stage I calcium carbonate morphology). Age control from Koning, 2009). 1–4 m thick.
5000
Kt
Tsx
TEMA
9000
Kc
Kclt
Kg
Kmd
Pg Kml
Kclt
Intrusion of brecciated, porphyritic trachyte of the Jackass Mountain Formation (lower Oligocene)—Similar to unit Tgjb but in sills, dikes, or
small plugs.
ish-gray to pale brown to light yellowish-brown to light brown. Redder hues are more prevalent on the Three Rivers fan and near the base of the
deposit. Sediment consists of clayey-silty very fine- to medium-grained sand interbedded with very thin to medium lenticular beds of medium- to very
coarse-grained sand, pebbly sand, and sandy pebbles. Most of the clayey to silty fine sand is internally massive and pedogenically modified
(marked by moderate ped development and Stage I gypsum accumulation); locally, there are minor laminations to thin beds. Scattered, minor
pebbles and medium to very coarse sand are present. Top soil characterized by a calcic horizon with Stage I to II carbonate morphology.
10000
Qls
Qa
Kc
Pag
Pg
Py
Tist
Qls
Kg
Kmd
Kml
TR
Ps
2000
TB-209
10000
11000
Manchester Spr
Carrizozo West quad
Carrizozo East quad
11000
East
Tsrs
P
N
New
Me
xic
o
S
West
MEXI
http://geoinfo.nmt.edu
A’’ Elevation
(ft)
Rhyolite to granite (Oligocene)—White to pale orange, aphanitic and typically aphyric, igneous rocks forming dikes, sills, and irregular igneous
masses north of Nogal. Where present, phenocrysts consist of <10% quartz. Unit includes intrusion of Vera Cruz Mountain of Rawling (2011). This
intrusion exhibits a core of biotite-phyric granite or syenite surrounded by aphyric trachyte and quartz-phyric trachyte. Commonly associated with
faults.
New Mexico Bureau of Geology and Mineral Resources
NEW M EXICO I NSTITUTE OF M INING AND TECHNOLOGY
801 Leroy Place, Socorro, New Mexico 87801-4796 (575) 835-5490
105°57'30"W
A’
Tsrqd
O
C
s
urce
eso
lR
ra
A
Elevation
(ft)
Intrusive rocks, undivided (Eocene to Oligocene)
STOCKS
by
33°15'0"N
Basalt of the Malpais (middle Holocene)—Gray, vesicular basalt that contains 5% phenocrysts of pyroxene (0.5–2.0 mm long). Groundmass is
0.1–0.3 mm and a mix of plagioclase and pyroxene(?). Up to several meters thick.
SIERRA BLANCA AND CAPITAN INTRUSIVE ROCKS
June 2014
106°0'0"W
Older basin fill of the Tularosa Basin, undivided (Miocene to lower Pliocene?)—Clayey-silty, very fine- to medium-grained sand interbedded
with minor conglomerate beds, locally with minor scattered medium- to very coarse-grained sand and 1–10% pebbles. Mapped south of the Three
Rivers drainage on the footwall of the Alamogordo fault. Unconformably lies beneath unit Qao1, and is distinguished from younger deposits by
smaller gravel sizes, common calcium carbonate-impregnation of gravel beds, strong consolidation, and steeper dips. Base is not exposed. Colors
of non-gravelly beds range from very pale brown to light yellowish-brown to light brown to pink. Paleosols are characterized by calcic horizons
(Stage II morphology in limited exposures) underlain by gypsic horizons; locally, the calcic horizons are overlain by thin, yellowish-red, illuviated
clay horizons. Greatest exposed thickness is 2 m, but unit is 120 m thick at the Lewelling #1 well (see cross section). On the immediate fault hanging
wall, basin-fill is up to ~700 m thick (see cross section).
QUATERNARY
Preliminary Geologic Map of the northeastern
Tularosa Basin and western Sierra Blanca Basin,
Lincoln and Otero Counties, New Mexico
106°2'30"W
High-level sandy gravels (Pliocene to lower Pleistocene)—Sandy gravel whose base is >15 m above present drainage bottoms and above straths
associated with Qao1. Unit not exposed, but surface gravel consist of pebbles and cobbles with 1–10% boulders. Where present, an eroded
horizon of relatively large clasts is used to map the base of this terrace deposit. 1–10 m-thick.
IGNEOUS AND VOLCANICLASTIC ROCKS
1:50,000
TA
south, with strong Stage III to IV calcic horizons more common to the north. Locally, a reddish-yellow Bw or Bt soil horizon overlies calcic horizons.
In places, such as along Willow Draw and Harkey Draw, surface erosion has resulted in a general lack of a notable calcic horizon. Weakly to
well consolidated. 3–12 m-thick.
In coarse channel fills, gravel is dominated by pebbles but cobbles and boulders are abundant close to the mountain front. Gravel is commonly
clast-supported and imbricated, but cobbly, massive debris flow beds locally fill paleochannels. Sand is mostly medium- to very coarse-grained.
280
EW
Older alluvium, undivided (Pleistocene)—Undifferentiated older alluvium recognized by its red hues, abundant gypsum, and locally well-developed, buried soils. To the south, rhizoliths commonly seen that are cemented by gypsum. There are varying proportions of gravelly channel-fills, in which gravel content decreases and sand content increases in a downstream direction; gravel dominates within 1–2 km of mountain
fronts. Gravel consists of pebbles, cobbles, and minor boulders. Top soil characterized by a reddish Bw or Bt horizon (where preserved), underlain
by horizons of Stage III to IV calcium carbonate and/or gypsum accumulation, with gypsum content increasing to the south. Base of unit generally
?not exposed. Unit is commonly overlain by younger, finer-grained sheetflood deposits, correlative to Qse. Well consolidated and up to 25 m thick.
Qao2
PERMIAN
250
New Mexico Bureau of Geology and Mineral Resources, Socorro, NM
Adjunct Faculty, Earth and Planetary Sciences Dept.,
University of New Mexico, Albuquerque, NM
Terrace gravel, undivided (Pleistocene)—Undifferentiated terrace deposits flanking major drainages. Composed primarily of sandy
pebbles–cobbles and lesser boulders. Straths located 3 to 15 m above local base level. In the southwest compilation map area, this unit was
applied to thin(?), highly gypsiferous deposits overlying erosional surfaces greater than 10 m above active drainages. Generally 0.5–2.0 m thick,
?but locally as thick as 5 m.
break and scale change
240
as isolated, matrix-supported clasts and in thin, discontinuous lenses. Larger dimension gravel beds are laterally continuous, well-bedded, and
clast-supported but matrix-rich; these may contain up to 10% cobbles. Locally contains gypsum rhizoliths or filaments. Topsoil marked by common,
macroscopic clay illuviation textures, rare disintegrating clasts, and Stage I+ to II+ carbonate morphology underlain by Stage I gypsum accumulation. Weakly to well consolidated 1–3(?) m thick.
Kc Younger allostratigraphic subunit of older alluvium (upper Pleistocene)—Sand and gravel inset into the middle subunit of older alluvium (Qao2),
CRETACEOUS
90
Daniel J. Koning 1, Shari Kelley 1, and Fraser Goff 2
Tsrs
Qao3
85
106°5'0"W
map scale. The oldest allostratigraphic subunit, mapped adjacent to steep mountain fronts (where it disconformably overlies Qai or Qao), consists
of brown pebbles and sands that are well-stratified to massive and typically fine upwards. Its topsoil is characterized by weak clay illuviation
textures
QTgand a Stage II to II+ carbonate morphology underlain by Stage I gypsum accumulations.
The second-oldest allostratigraphic unit is the most laterally extensive and locally inset into the oldest allostratigraphic unit. It commonly is brownish-gray to pale brown to light yellowish-brown to light brown. Redder hues are more prevalent on the Three Rivers fan and near the base of the
? ?
deposit.
Sediment consists of clayey-silty very fine- to medium-grained sand interbedded with very thin to medium lenticular beds of medium- to very
?
?
coarse-grained
sand, pebbly sand, and sandy pebbles. Most of the clayey to silty fine sand is internally massive and pedogenically modified
Tbf by moderate ped development and Stage I gypsum accumulation); locally, there are minor laminations to thin beds. Scattered, minor
(marked
Tsrssand are present. Top soil characterized by a calcic horizon with Stage I to II carbonate morphology.
? ?
pebbles
and medium
to very coarse
Tgjvs
Qtg
55
106°7'30"W
where Qar and Qay could not be differentiated at this map scale.
Qai
19
Qay
Qayr
af
Qao3
Qao
Kc 16 af
Kc
Qao2
12
18
27
Qay
19
Qao
Kg
Tist
Qao3
Qao1
Kg
10
Qao3
Ts
Twh
12
Qse
Kg
Qao1
Qao1
Twh
15
14
Qse
Tid
Twh
Qao2
Qay
Qao Kg Qao1 QaoQct
33
41
Tid16
Kg QTg
Qao2
3
Kg
Qay
Kclt
Qao3
Qao2
Kg
Twh
Tist Kg Kg
af
Qay
QTg
10
Kclt Kg Qdsct
af
Qao3
Qao Qao
Qay
Twtr
QayQay
Qao1
Qao
Kg
Qao3
Qao3
Kg
Qao
Qayr
Qao3
Qao1
85
Qao3
Qao2
6
Qay KmdKg7 97
Qay
QayQay
Qao3
Qay
10
10
Qao2
Qar Qay
Qao3
Qao1 Qao1
Twh
Qay
Kclt
Qay
10
Qao2
Qar
Qayr
Qar
8 Tirg
Qay
Qar
Qar
9
Kmd
Qayr Qao2
17
Qao1
Qao1
Qao3
Qao2
Kmd
Qao2
33°35'0"N
Qay
7
af
Qay
15
Twh
Qls
Qar
Qao1
Twh
Tist
Qay
Tid
Qao1
Qbm
7
14
Qay
Qse
14
Qao2
Qao1
Qao
Qar
Qao1
Twh
Tist
Qao1Qao1
QaiQao Kg
Qao2
Qayr
Qayr
10
Qao2
Qao2
Twh
Kc
Qay
Qse Qao1
Qayr
Qao1
Qay
Qao Qao Qao
Qse
Qao2
Qay
Qay
Tist 5
Qao2
Qay
77
Tid
Tist
QseQse
2
75
33°35'0"N
Qao2Qay
Twtr
35
Twh
TistKmd
Qao
Qayr
Qao2
Qay Twtr
Qay Twh Qao1
Qao1
Qay
Qao3
18
Qar
Qay
Qao2
Qay
16
13
Qay
af Qao3 Qao3
13
32 Qao
Qse
Qay
Tist Qct
Qay
Qayr
Kd6
Qay
Qay
Qayr
Qao3
Qay
Qao3
Twh
Qao2
Kg
Qao2
QarQay
Qay
Tist
12
QaoTistQao
Tid
Qao3
Qao1
Qar
7 Qao1 6Kg KmdKg
QaiQai
Qao3
Qao2 Qay
Qar
Qao2
Qao1
Tist
Twtr
Twtr
Tist
Qbm
TQao
ist
Qay
Qao2 78 Qao1
Qbm
Qao2
Twh
Kc
Twtr
Tid
9
Twtr
Kc
Qao3
Qao
Qao3
13
Tist
Tirg
Twh
Qayr
Qay
Qbm
10
Qar
Qao
Tist
Twtr
Twtr
Qay
Qdsct
Qao2
Qao2
Qao1
Qao3
Qls
Qao2Qao1
13
Qao2
Qay
Kmd QaoQao
Qao2 Qay
Qay Twh
Qao3
Qao
Kmd QaoKmd
Qao2
Qay
7
KmdKmd
Tid
Qay
Qayr
Qai
Qao1
Kmd
Qay
Qao2
Tc Kc
Qao
Qayr
Kg
Qay
7
Qay
8
Kg
5 Kmd Qao Kclt 8 11
Twh
Qao2 Qao2 Twtr
Qao1Qar
Tist
2
Tid
Qayr
Qay
Twh
TitaTita
Qar
Twtat
Kmd6 10Qls13
Qay
Qao
Qao1
9 Kc
Qao2
Qao3
14
5
13 Qayr
Qay
Qao3Twh
Kg 6
Qao
Qayr
Tc
Qayr
Qay
Kc 32
Qayr Twtat
38
Twh
Kc
5
Twtr
Qay
Qay
Twtr
Twtr
Qao1
Qar
Qao1
Twtr
14
Qao2
Qay
Qse
Qse
Kc QaoQao Qay
Tc
Qct
Twtr
Tid
6
Twtr
8
Qao
Qay
Qay
Qao1
Qar
Qar
Qls
5
Twtat 15
Qao3
Qao3
Twtr
Qct
Qao1
Qay Qay
Qay
Kclt
Qse
Qay
46
Tc
5 13
Twh
Twh
Qao1
45
Qao1
5
15
Qao2
af
Qdsct
Qay
36
5
Qao1
Qay
4
Qao1
QTgQTg
Qct Qao1
Psr
Qay
14 10
10
Qao2
Kc
Qao3 Tc
Kc
Qai
Qay
15
Qao2
Twtt
Kclt
Qao1
Qay
Qay
Qao
Qao1
af
Qao1
6
1728 20
Qay
Twtr
Qayr Timd
Tita
Kg34
Kd
Qar
Timd
Qao2 Twtr
Qay
Qay
Timd
Kmd
23
Kg
8
Qay
4
Qbm
Qse
11
Qayr
Qao
7 13
Qao2
Twtr Qayr
Kclt
Kg
Qayr
3
Qse
Qay
4 Qao1
Qay
Tc
Kc
Twtat
15
Qao2
Qay
Twtt
Qao
Qai
2117
Qay
Qao
Qdsct Twtt
Qay
Kmd
Qct
Qao3
Kc
Qao1
Qse
Qao3
Qdsct
Qao1
Kc
6
Twtat
Kc
^m 12
Qdsct
Qary
Kc
23
7 Qls
79
12
Twtat
QTg
Qdsct
27
Psr
Timd
26
Tist
Qao2
Qao3
9
Qdsct
Kg
Kc
Qao1
Qay
Twtat
Qao
8
Qao1
Qay
22
Qct Qao2
9
Qayr
Qao2
af
32
QdsctQao1
Qay
Qse 14
Qse Tita7 9
^m
Qct
Qct
21
14
Qay
40
Qay
Qao1
Qao
Qao3
Qao3
Qar
9
Kc
Twtat
49
Tc Qao3
Tid
10
24 19
Qct Qao 13Qao3
Twtt
Qar
5
Qse
Kc
Qay
Kclt
12
Kc
65QseKg
Pag
Twtat
15
Kclt
Qay
Qai
Qao3
34
Qar
16
Tist
Tc
Qay
Tist
Qao2
Twtr
Qse
Qay
Kc
Qse
Tist
Qay
Kc
Qao
14
Qao3
Qse
Qao1
Qct
Qay
Qao2
Kclt
QarKc
Pag
23
16
Qao1
Twtat
Kg
Qay
Qao 6
25
26
Kc
Pag
26
Qao
23
Tist
Twtat Twtr
19
30
11
23
27
Kg
30
Tist Qao3
29
Pag
22
26
QayKc
Psr
7
Qse5
Qdsct
Qse/Kc
Qay
Qay
32
Qao3 Kclt Tist Qao3
Qay
16
12
Tita
30
Qay
Tcp
71
Twtr
41
Psr
Psr
KcQao3
24 Twtt Qdsct
Qao2
74
Qao1
12 Qao1 Kclt
9
15
21
Kc
Twtat
Tita
15
23
Tc
Twh
Qct
Kclt
Qct
Qao1Qar
15
Qse
Qao3
Qao2
8
14
Qao3 Qay
Qct
28
Qar Qay
Qao1
5Tita
Kc
Twtr
12
10
Pag
Qao1
Qar
Qar
Tist
Qao3
Qay
Qay
Twtd
Qao1
Kc
Pag
8
Qao
Qao2
Kd 11
Kc
10
Qao3
Qay
Tita
Qayr
Qayr
Qse
Qct
Qao2
7
Ts
KcKc Qao1
23
12
Qct
Qay
Ti
9
Qayr
Kg
Kc Tita
Qct
Qao
Qao3 Qao1
29
Qayr
Qay
Twh
20
17
Twtd
Kc
Kt
Kmd
10
18
Tist
^m6
Qse
Qao2
Qay
Kc
Qay QaoQao1
Qao
Kc
6
Kclt
Qay
Qay
Ts
9
24 28
Qao2
24
Qbm
17
Qao3
Qayr
Kc
29
Pag
7
Kg
Kmd
Qao1
Qct
Qao1
QTg
14
Qao2
Twtr
Twtr
11
Kc
6
Twh
8
1515Qao1
Qct 59
Qar
Twh
Qao1Kc
Qao3Ts
10 QTg
Qao2
^m
Qay
Qai
QayQay Qayr
Qao3
1210 Qay
14
Qay
Tist
Qct
Kc Qao1
QTg
Kc
Qse
Qao1
30
25
Twtat
Tita
Qao1
Qayr
5
Qao2
36
Qse
TsQay 17
Kc
5
Qbm
Qay
Qao1
Qct
Qbm
Qay
Qls
Kc
Kd
19
Qao
23
QTg
13
Qay
16
13
Qao2
10 17
Qse
Qayr Qay
Twtd
Qay
Tid
64
Qao1
26
Qao
Tcp
22
Twtat
35
28
40
Tist18
Qao3 Qay 16
Tcp18
Tist
Qay
Kd
Qao
Qao2Qay
34
20
Qay
Qao2
Qayr
Qao
Qct
Kc
21
29
Qct
Tist
Kc
14
14
Qdsct
Qse
23
Psr
Qse/Kc
8
Kmd
30 10
Qls 20 Qao1 Qao
Qay
Qao1
Qbm
14
27
Qdsct
Qao2
Qay
20
Qay Qao1
Qls
Tc
18
Qao1
Twh
Kc
^m
Tcp
20
Kt Qct
Qse
Qao1
Twh
Qay
24
Twtd
Qse/Kc
7
25Qao1
Qao
Qct
Kc
Twh
39
Kd
Kc
17
Qao1
5Tc
Qls
21
9 Qay Qao
Kc
Kmd
Qay
13
Qao2
18
Qct
3
Qse
Kc
Qls
Qao1
Twt
10
Qse/Tc
13
Pag
Qse/Kc
Tc
Qayr
25
QbmQbm Qay Qse
Qct
Qct
Qao1
Kc
Qay
Qay
Kc
8
18
12
5
Qao2
Qay
Qao2
Qao1
Kc
Kg
4
Tc
^m
Kc
Qbm
Qct
Qse
Tc Qse/Tc
Pag
23 Tcp
Qls
37
15
Qao2
1214Tist
Qayr
13
18
Tist
Kc
Qbm
33°32'30"N
10
Qls
Qse
8
24
Qbm
Tc
14
Kc
Qls
37
^m
Qayr
Qay
20
Qls
Qao
Kd
Qbm
Kclt Qay
Qbm
Qct 14Qct
19
19
Qay
Qbm Qay
Qay
Qao2
16Tist
Qbm
Kc
Qay
1323
Qbm
Qay
Kt21
23
6
Ts 11 2383
Qay
Qbm
Tc
Qar
11
Qay
45
Qay
Kg 18
Qao2
10 22
Tc
34
Titd
Qay
39
Tc
Qao 18
Kg Kclt
Kc
Qay
33°32'30"N
46
4116
80
Twtd
48
Tc Qao
Qct Qao2
Kg Kclt Tist
22
Ts
Qay
Qao1
Tist
Twbpt
Qay
Qay Qse
33
Qay
Kc
Qay
Qar
Qay
22
Tist
Qao2
50 50
Qse/Kc
Tc
Kmd
Qay Twh
8
17 Kc Qao1 Qct
Qct
8 ^m
Qao
Qay
13 12 Qls
Qao
Qct
Qao
Qay
17
74
Qse/Kc
Titd
Tc
Qdsct
Kg
Qay
Kmd
Kclt
24
Qay
Qar
Qayr
10
19
Qay
Kc
8
Qay
Tc
Ts
Tc
Qay
Titd
Qao3
Qao3
Qtg
Qay
Qao
Tist
Qao
Qao Qtg QaoQao
TwtdQao
Kmd
Twtd
Qdsct
Qai
Tist
Qao
af Qao3Qao3
Qao2
Twtd
Ts
Qtg
Qao3
Qao
Qay
Tc
15
Qay
Kclt
Qct
Qao Qtg
Qao
Qao
Qdsct
Kg 19Kclt
^m
Qao2
Qao
Qay
Qai Qai Qai
Qct
Tist
Qct
26
Qay
Qse
Kc
Qao3
Twt
Qay
Ts
19
Qay
9
Qao1
Qao
Tc
Psr Qay
Tist
Qao2
Kc
Qtg
Qao2
Qao1
Ts
9
Qao
Qao
15
Tc
^m
Qls
Twt
Qay af
Qao1
Qao Qtg
Qay 10
Qdsct
Qay
Qao2 Qayr
Qct Twt
Ts
Qse
Qar
5
Tsrs Twtr
Qao1
Tc
Qao3
Qao1
Qao Qao
Qay QayQao1
Tist
Qay
Qao1
Qao1 Kc
Qar
Twt
Twt Twtr Twt TsrqdQao
Tsrs
Qct
19 Tc
Qay
Qay
Qao1
Twt
Qay
Qay
Qao3
Qar
Qay
Tc
Qay
Kclt
Qse
Twtr
Qao1
Twtat
Qai
Kc
Twtat
14
18
Qao1
Qar
Qay
QTg
32
Qay
9
Twt
Tc
Qay
TsrsTsx
Ts
20
Tsx
Twt
Ts
Qao120 Qao1
Qao1
Twt
14
Tc Qct
Tc
Kc
Qao
Kd
23
Twbpt
Qay
Qai Qar
Qao
16
Qls Qao2
Twt
Ts KcKc
Qay
Titb
Qao
Twtat
Twt
Kc
Twt
Tist
Ts
Qai
Qay
Qay
Qay
TcTc
Qao
Qao Tc
Tc
Twt
Twt
12
Ts 914
Kc
19
Ts Ts Ts
11
Tkgf
Qay
Qay
Qao
Qao1Qao1
Qao1
Qao3
Tc
Kc
Tc
26Ts Tc
TcQao Ts
Qls
Kc12
Qao3
Qao2
Tc
Qao2
Tsx
Qao
Ts
Kc
Ts65
Tsx
Tist
Twt
Qao1
Qay
Qao1
Qao2
Qay
Qao
Twt
Qse/Kc
Titd
57
Qct
Qao2
Qar
Qao
Qao
Tc 9
Tist
Twtd
Kc
Kg16
TcKc
Twt 105°42'30"W
Tsx
Tsx
Tc
Ts
Kc QayQao2
Tist
Kc Qao2
Tsrs
Twt Twt
Qao
12
Qao1
Qay
Tsx
14
Qao1
Qay
21
Qai
Qay Qao
Twt
Twt
Qay
Qao2 Qay
Qse/Kc
Qao1
Qay
Tkgf
Kclt Kc
Tkgf
Qao
Kc
36
Qct
Qay
Kmd
Qao
Qayr
Qao2
Qao2
Qao2
Qay
Qtg
Tc
Qao2
Kg
Qay2037
Qse/Tc
Tsx Twt
Qse
Qao2
Qse
Tc
10
Qao2
Qao2
Twt Qct
Qai Qay
TcQay
Tkgf
15
Qay Qay
Qay 21
Qay
Kclt
Kc
Qar Qay
QtgQay
Tsx
Ts
Qse Qao2
Qay
Qayr Qai
Tsrs
Qse/Kc
Qao2Ts
QTg
Qao
Qao2
Qay
Kml
Qao2
Qao2
Qay
Qct
Qao1
Twh
Twh
Tc
Tc
Kc
Qse/Tc
QayTwt
6
9 Qct
Ts
Qao2
Qay
34
Qao1
Qayr
Qay
Kt
Qay
5
6
Qay
Twtat
Qao
Qct
Tsrs
Ts
Tc
Qay
Twt
7
Twt
Qct
63
Qao1
Ts
6
Twtr
Qay Qtg
Tc
Tita
7
Qao2
Qao1
Twtr
5
Qao2
Qao3
Kc
Qay
31
Qay
Qay Kc
Twt Tsrs
Tc
QtgQay 70
Twtat Twtr
Qay
Qao2
6
Kc
5 Qay
Qao Qao
Qao3
Tc 11 Tc
Qao2
Qar
12
Qao2
Tc
7
Qao3
15 10
Qay
Ts
10Kc QayQay 13
Twh
7 Qai Qao1
12
35
Qao2
Qse/Tc
Tsrs
Twtat?
Qay
Qay
27 Tist
Qay
Qay
Qayr
Qct
Ts
Qao2
Qao2
Qse
Twt
Tsx
Tc
5
Qao2
Tc
Qar
Qao2
Tc
Qao3
Qar
Qayr
9
Qao1
9 Qao2
Qay
Qao2
Qao1 Qay
11
Twt
Tc
Tc Qay QtgQay
Qay
Tsx
Tc TcQao1
6 1410
Qao1
Qse/Kc
77
Tist
Qayr
Twtat
14Qay
KgKg
Qao3
Twh
10
5
Tsrs
Twtat Twtr
Kc
10 18Qay
8 Qay
Tist
Qay
Tkgf
Tc
Qar
Kg
10
10
Twt
Ts
Kml
Qse/Tc
5
12
Qao1
Qay
Tsrs
12
Twtr
Tc
Qtg
7
Twt
Twt
Qao1Qao2
TcTc
Twtt
Qao3
Tsrs
Qar
Tist
Twtt
Tist
5
Qay
Qao2 21
QayTcTc
Qay
Twt
11 9
Qay
Qay
Qse/Kc
Ts Ts
Qay
6
Twt
9
Qao2
Ts
Qao2
Qay
Kg
Qayr
Twt
Kclt
Tim
5
Tsx
2
2
Qse/Tc
Qay Tc10
Qao3
40
Twt
Qay
17
9
Qao2 Qao37
1312 Qtg
Twh
34
17
Qay
Qay
Qay
TwtTwtTwt Twt
TsQao3
10
Qay
15
Twtt
Qay
9Qar
Twtat
14
QayQtg Qay
Qao2
Ts
Qay Ts
Kt TimQao1 Qao2
Tsx Twt
Qao2
Qay
Tsx
^m
Tnpt
66
Tsrs
QayTs
Ts
Qay
53
12
Qse/Kc Qao2
Ts
Qao2
Tnpt
8
Qao1
Qct
Twt
30 8Qay
Qao1
Qao2
Qao2
47
14
Ts
Ts
Qay
Qao2
Tsrqd
Qay
10
7Qar
Tist
Qay
Twbpt
8
6Qao2
TitbQay
Kmd
Tsx TsxTwtr
Kc
Qse/Kc
Tc 11
Qao2
Twbpt Twtd
Twbpt
Qay Kg
Qao1 Qay
Twt
Twt
Qse
Twbpt
7Qao2
10
Qao3
Kd 36 Qar
Twtr
Tc 14
Qar
Qao2
Kc
Qao1
Qay
Qao2
Kt
Twt
Tsx
Ts11
Qay Qao3
Tnpt Twt Tsx
Twtat
Qay
9Ts
Kml
11
20
Qao2 Qao1
Qao3 Qao2
Tsrs
Qao2
18
Qao2
Twbpt
Tc
Kc
Kml
14
Twt
Qay
Qay
Tsrs
Qao1
Qct
Qay
Qct Kml
QayQayr
Twtt Ts
Qse/Tc
Ts Qar
Qse
30
Ts
Twbpt?
Tc
Twt
Tsx
Tist
QayKc
Ts
Qao2
19
Twtat
Qay
Kt 16
Tim
Qao2
Twt
Qao2
Qao2
Kc Kc Qls
910
Kc
Twt
Twtd
Qay
KtQao1
Kclt
14
Qayr
Qao2
Qay
Qar
Qay
Qao
Twt
Qao2
Qao
Qay
Ts
Qse/Tc
Qao2
44
Ts
Kmd
Qao1
Qay
Qse
Kc
Twt
Qse/Kc
Ts
Qao2
Qayr
Tist
Qct
Qay
17
QayTs
Ts Ts
Qai
Qse
Qay
Qar
Qar
Qse/Kc
Qay Tita Twtr
Qao1
Twh
Ts
Qao1
Qao2
Twh Qay
Kc7
Qao1Qse/Tc
Qct
Qar
Twt
Qay
Tsx
Qse
Qse/Kc
20
Qay
26
Qayr
Ts
Twt
Qay
Qao2
21
8
Qse/Tc
Qay
Ts
16Qao2 Qay
Twt
Kc
55 13
Tist
Qay
Twh TwttQao2
Qay Qay
Qse/Tc Qay
Qao2
Qay
10
Qdsct
44
Tsrqd
21
Tist
Qay Qay
33°30'0"N
Tsrqd
Tsrs
Qay
Tist
Ts52 40 Ts
Tsrs
7Tc
Qayr
Qay
Tist
Ts
Kd
Qao1
Qao2
10
Qayr
Qao2
Qay
Qay
Qay Qse
Qayr
Qao2 Qay/Qai Qao2
Qar
Qai
Qai
Qay
Twtt
Twt
Qay TimQse
Qay
Ts 11
Twt Tsrqd
Twtr
Ts
Ts
Qao2
Qay
Qct
Qay
Qao1
^m
Qay
Tist
75
5
Qao1
Qao1
Tsrs
Tsrs
Twh
Twtat
Qar
Tist
7
Tc
Qao2
Tsrs
Qay
Qay
80
Qay
Qao2
Qay
Tist
Qct
Qay
Ts
Tsrqd
Tc
Twtt
Twtd
Twbpt
Qay
Twt
Ts
28
Qct
Twt
Qao2
Qct
Qay
Qai Qay Qay
Tsx
Qai
Qao1
Qct
Qct
Qct
Twt
Qay
Tsrqd
Tsrqd
Qao1
Qao2
Qao2
Tnpt
Qct
Twtd
Tist
Qar
Tsrqd
Ts
Tsrqd
Qao
Qao1
Tsrs
Qao
Tsrs
Qct
Qay
Tsx
Tsrs
Qao1
Tist
Tsrs
Qao1
Qse
Tsrs
33°30'0"N
Qse
Qay
Qayr
Qay
Tsrs
Ts Ts
Qct
Qay
TistTist
Twtr
Qao Qayr Timd
Qao1
Ts
Twtd
Qay
Twbpt
Qdsct
Qayr
Qay
KdQay
Qao2
Tc Ts TcQay
Qao2
Qay
Tsrqd
Tist
Qar
Qao2
Twtr
^m
Qayr
Ts
Qct
Ts Ts
Qai
105°45'0"W
Qayr
Kc
Qay QTgTc
Qls
Ts
Qao2
Tsrs Twt Twtr
Twh
Tsrqd
Qar
Qay/Qai
Qse
Tnt
Qay
Twtat
Qao
Qao1
Qao2
5
12
Tsrqd
Tsrqd
Tc
13
Qao2
TwtrQao
Qao1
Qay
QTg 10
^m
86
Qay
Qay
Tc
Tim
^m
Ts
Qao
Twh Twtt
Qao
Qay Qao
8
4
Qayr
QayrQao2
Qao Twtr
Qay Qay Qay/Qai Qao2
Qay/Qai Ts
Qay
15
Qay
Qao1
Twbpt
Tsrqd
TcQct
Twtt
6
15 Tsrqd Tsrs
Qay
^m Qao2
Qar
Qse
TcQay Qay
15
Ts Ts Qayr Qao2
10
Qay/Qai
6
Qayr
Tsrqd
Qao2
Qay
Qao2
Qse
Qar
Kml
Qao1
Timd
TsrqdTsx Tsx Tsrqd
Qay Qai
QTg Qay
Qao2
^m
Qay
Qao2
Qse
29
Twt
Qct
Qgy 6 Kd
Tc
10
Qao2TitaQay
Tsrs
Qao2
Tsrqd
Twtt Qao2
27
Tsrqd
71
Qay
TcQTg
Qao2
Twtd Tnt
afe
5
Qgy
Qct
Qay
Tc
Qgy Qao2
58^m
25
Qar
Qay
16
Qdsct
Twh
Qay
Qgy
Kd
Qay/Qai
Tsrqd
73
Qse
Twtt
Qay
Qtr
Tgl
Twtd
Qao2
Ts
20
Twtt
Twt
Twh
Qgy
Qao2
Qgy
QTg
Tigjb
Twbpt
Twt Tnt
Kd
Qao2Twtt
Tc
Qao2 22
12
Twtt
60
85
Qay
6
Tsrqd
Qct
Tsrqd
TwttTita
80
Qtr Qse Qay
Tgjpt Qay
Qse
3
Qayr
Qar
Qar
Qay
28
Qao2 Qtr
Qay
Qao2 Qgy
19 Tist 15
Tgjb
Qay
Ts
Tsx
Twtat
30Qay
Qao2
Qay
62Qay
Timd Tnt
QayTwtr
Ts
24
14
Qayr
Kg Kmd
32
15 75
Qgy
Qct
Twtd
43
Tigjb Qay Qay/Qai
Qao2
Twtt
Qayr
Twtr
Twh
Qay
Qayr
Twtr
QTg
9
Tsrqd
Tsrqd
Twtt
Qse/Kc
24
Qar
6
Qct
8
Qao2
34
80
Tgjta
31
31
QaoQao2
86
Qao1
Qao2
Qar
32
30
Qao2 Qao2
Qao2
5
QTg
Qayr
Kc
4
Tc
Tist
Tsrqd
Kg Qao
Qct
Tgl
Kg
Qay
QTg
Qayr
Kd
Kml 72
KmdQao2
Tsrqd
Qar
Twtr Twtt
2827 Qao
Twt
Tid Ts
TglTita Twtt
Qao2 Qse/Kc Qse/Kc Qse
30
Qgy
Qao2
Qay
Qar
Ts
Twtr 72
Qct Tigjb
Qct
33
Qayr
Qao2
Qao2 Qao1
Qao2
Tigjb
Qay Qao2
87
QaoKd^m
Tsrqd
Qct
Qay
Qay
Qao1
Qao1 Qse/Kc
Tsrqd
Kd
10
Qar Twbpt Qay Twtt Qay
Tsrqd
7
Qai Qay
Qse/Kc
Ts
Qao
Twtd
Twtt
afe
Twh
26
Qao2
86
Qao
Qao2
Tsrqd
Qct
Qao1
Qayr
Tgl
Qao1
Tita
Qao
Qao1 Qao1
Twtt
Qay
Kd
Twbpt
Twtt
Twtt
Titd
Qay
Tsrs
Qse/Kc
Tgjb
Tsrqd
Qay/Qai
Twtt
Qay
Twt
Qay
Kt
Qao
Qay
Kmd Kml
Qdsct
QTg
Qay Qay
Tgl
Kd
Twbpt
4
12
Qct
Qayr
Qar
Twbpt
Qao2
Tsrqd
Qct
Kml
Tgl Tgl
Qao
Tsrs
Qao2
Kt
Qao1
Tsrqd Qtg
Kt
5
4
Qar
Kml
Kd^m
Twtt
Qao2
Kml
Qao1
TwttTwttTwbpt
Twh
Description of Map Units
Qao1
Twt
Tgl Tgjpt Qao2
12
Qay/Qai Qay
80
Qao2Kmd
Tsrqd
Titd Titd
Qao1
12
8
17
Qay
Qao2 Qao2 Qao2
Tsrqd Tsrs Qct
Qao1
Qao2 Twh
Qay
Twh
Qay
15
38Qao1
11 Qao2
Twtat
Titd
Qay Qar
Twtt
QarQao2 Qct
Qay
73
Tc
12
Ts
Qls
Qay
Qao2
Qay
Qao2
Qao1
^m
Qao1
Tita
Qar
Tsrqd
14
Qar
Twtr
Qao2
Qao1
80
Qao1
61
Twtat
Qao2
Kmd
Qay
Qao1
Tsrs
Qao2
Qao2
Qay62
Tsb
Kml
Qay
30Ts
Qay
Qao2
Qao1
15
Qls
Twtat
^m
^mQay Qao1
TwttTwbpt Tgjb
5
Qtg Tsrs
Qao2
Pag
Qay
Qao2
Qao1
Twt
Qay
The units described below were mapped by field traverses and inspection of aerial photography. Grain sizes follow the Udden–Wentworth scale
Twtr Twtr Qct
Qay
Tgjta
55^m
6
Qao2
Qay
Tsrs
Qao1
Qao2
Qao2
82
Qao2
QayrQao1
Twbpt
Twtt Qay
Tsrqd
Qay
Qay
^m
3
9
84
Kt
5
Qao2
Qao2
Qao2
Tsrs
Kmd
Qar
Kd
Twtt Twt
Qay
Twh
Qay
Qao2
Qay
Qao2
Qay
Qao2
Qao2
Qao2
QTgQay
for clastic sediments (Udden, 1914; Wentworth, 1922) and are based on field estimates. Pebbles are subdivided as shown in Compton (1985).
Qdsct Qao2
Ts
Qao2
Tsrqd
Twt
Tgl
22
Kt
Qao1
Tgjpt
10
Qar
80
Titb
Timd
Twtat
Timd
TwttQao1
Qao2
QTgKmd
Qar
Qao1 Qao2
Tsrqd Tsrqd
3
13 Qao1
Qao2
Timd
Twh
Qao2
Kmd
Qao2 Qao2
Qar Qay Qar Qayr
QayQay
Qct
Qao2
^m ^m
Qao2 Qao2 23
Tsrqd
Pag
Twt
Pag
2597 Qao1 ^m
Twt
Qay
Qao2
Tsrs
Qay
Kmd
Qayr
The term “clast(s)” refers to the grain size fraction greater than 2 mm in diameter. Descriptions of bedding thickness follow Ingram (1954). Colors
Twt
Qct
Qay
Tsrqd
8
Twtr
Qct
Qay
Qct
13
Tc
Qay
Tsrs
QTg
Twt
12
Twt
Twt
Twbpt
Qao2
Qayr
Qay
Qay
81
^m Kd
37 Qay
Qao2
Twt Twt Twt
Qao2
Pag
Qao2
Twh
QTg
Tsrqd
Twtr
Qao2 Qao2
Twt
Qls Tgjpt Tgl
Kd
Qct
Qay
Qay
Qao1
Twh
TwtrTwbpt
Qay
Pag 66 Qao2 Kd
Qao2
Timd
TsrqdTwt
Qao2 Qao2
Twtt
Tsrqd Timd
Tid
of sediment are based on visual comparison of dry samples to the Munsell Soil Color Charts (Munsell Color, 1994). Soil horizon designations and
8
Qct
10
Qtg
Tsrs
Twt
Qdsct
5
Twh
14
Qay
6
Twtt
Twt
Twt
^m
Kd
Twh
Pag
Qao2Kmd
Qao2
Qay
Qao2
Tsrs
56Qao2
Tsrqd
Kd Kt 59
Twtr Qao1 Twtt
Qct
Qct
Qao2
Qao1
Ts Twh
Qls
Qay Twh
Tsrqd
Pag
Ts
Qao2
Qay
Qdsct
Qao2
Tsrs
Tid
Qay
Twt
Ts
Kmd
descriptive terms follow those of the Soil Survey Staff (1992), Birkeland et al. (1991), and Birkeland (1999). Stages of pedogenic calcium carbonQay
Ts
Kd 85 Qay
77
59 Qar Twtr
Qay
Twbpt
Qao2 Qar Qao2Qct
Qay
Twt
Qao2 Qay 9 Pag
PsfPag
Qao2
Twtr
Qay
Qao1
Qdsct
26
Qao2
Qay
TwttQls Tgjb
Tist
Qls
TcTcQao2
Twh
Kmd
Twtr
Tsrqd
Qao2
Qay
Qao2
Tsrs
3
Qao2
24 Qct
QseKd
Qao2
Qay
Qao2
7
9
4
Kd
Qay
Twtr
15
Tgjb
Kg
ate morphology follow those of Gile et al. (1966) and Birkeland (1999). Except where noted, description of sedimentary and igneous rocks was
16
Tist
13
Qct Timd
Qct
Kd
3
13
Twt
Twtr
Tsrqd
Twh
Qay
Tc Tc
Tc
Tgjt
Qao2
Qao1
Qay Ts 15 Qao2
Qay
Tgjb Qdsct
Qao2 Twtr
80 Twt 80 Qtg
Qao2
Ts Qec43
Psf
Tsrs
Qay Qao2
Qayr
77
Twt
Twh
8
Tc
based on inspection using a hand lens. More detailed descriptions of lithology, presentation of age-related data, and discussion of depositional
Tc
Twh
Twtt
6 Kd
Qay
Ts
Qayr
4
Ts
afe
Twh
Qao2
Twt
afe
Qar
Tist
Tist
Qao2
Qay
Qct
Qao2
Qct
Tws Tist
77
64
Qct
Tsrs
22 Qao2
Ts Qls
Qao2
Tist
Qao2
TcQTg
Qay Qse/Kc
Qdsct
Qay
Qao2
TsQay
Kmd
Qao2
Qao2
Qay
environments are found in the accompanying report.
Twtt
Tgjpt
Tist
Qao
Qtg
QTg
Tsrs
Qay
Qay
32
Qao1
QctTwtr Qct
Qayr
Qls
Qao2
Ts
Qao2
Qse/Kc
Twh
9
TsQao2
Qay
2
Qay
25
52 Twh Qay
Tgjpt
QayrQao2
QdsctTs
Tsrs
Qayr
Kg8 26
70
Qct
Tgjt
Ts
Timd Tist
Twtr
Qdsct
Qao2 Kc
Qao2
Twtt
Ts
Twtt
Qar
Qse
Twt
Qdsct
Twh
Qao2
Qay
Qao2
Qao2
Qao3
Qao2
Tgjb Tgl
8
Twtt
Qay
8
Qse/Kg
Tsrs Qay
37
Tsrqd
52
Qct
16 Qao2Qao2
88
Qls Qct
Ts Qdsct
Qao2
Qay
Qao2
Tsrqd Tsrs
8
5
Tsrs
QayTwtt Tgl
Kmd
Tgjb
Kc Qec
Qao2
Qao2 Qao2
Qao3
Qao1
10
KgQao2 Kclt
Qct
Kc
Timd
For sedimentary units, a brief discussion is warranted on the difference between lithostratigraphic and allostratigraphic units. Most map units
5 3
75
Qec
Kc
45
Qao2
Tim
Qao2
8
11
Twtr
Qct 40
Kg
Qec
Qay
Qse/Kc
Twtt
Twtr
Qed
Tita
Timd
Qay
Tsb
Qay
Twtr
Twh
33°27'30"N
Tsrqd
Kg
Qse/Kmd
Qao2
Tgjt
Twtr
Kg
Qao2
Kc
Twtt
Tist
afe
Tim
Twbpt
5
Kmd TitaKclt
Qao2
Qao2
Qao2
presented below are lithostratigraphic, or are recognized by their geomorphic position or the inferred geomorphic process responsible for deposiQse
Twtr
Qay
Qao1
55
Qec Qay
5 80
Twh
Twtt
Tgjt Tgjpt
Twtr
Twh Twtr
Qec
Qse/Kg Kclt
Qayr
Qao2
Qao2
Tim
Qao1
42
Tita
80
Tita
Twh
Twbpt
Qar
Twtr Twtr
Tsb
Qao2
Qsec
Tita
33°27'30"N
tion. Lithostratigraphic units can be differentiated by lithologic properties (such as texture, color, and composition). Some Quaternary lithostratiQar
5
Kd
Qse/KcKc
10
afe
Qay
Twbpt
Twtr
Qayr
Qay
Kc
3
Qao1
Twtt Qao1
Qay
Qayr
Qay
Qao
Tita
Tim
KcKc Kc
Qao1
Qao2
Timd
Qayr
Qao2
Qay
Qse/Kmd
Timd
Twh
Twbpt
Qao1
Twtr 17 16
QayQay
Qay
Qct
Twtr
Qayr
Tgl
Twtt
Qao3
graphic units are subdivided into allostratigraphic units, which are separated by interpreted unconformable contacts or by inset relations (both
85
Tgjpt
Twtr
Ts
Qao2
25
6
Qao2
Qao2
Psf
afe
Twh
Qar
Twtt
Twtt
Qayr
Qar
Qao3
Qay
82
Twtt
Qay Tim
Psf
Tita
Kc afe
9
Twh
Twh
Qay Qay
Qao2
Twbpt
Qayr
18
Ti
Qao2
8
Qao2
Twtr
8
Qao3
Qay
Qao2afe
Qao1
Twbpt
representing inferred time gaps), as well as geomorphic position. Allostratigraphic units have numbers at the end of their map labels. For example,
Tgl
Twtt
Qse
67
Qao2
Twbpt
Qao2
Qao
Qao2
Qay
Psf
Qao2
75
Qao
Qay
30
Qao2
34
Qao1
Twh Twtr
Qao2
Tirt Timd
Twtt Qao2
30 Twh Ts
af
Qay
14
Qao3
Twh
Qao1
47
Twh Twh
Qao2
Qay
Qao2
Qse
lithostratigraphic unit Qao is subdivided into allostratigraphic units Qao3, Qao2, Qao1. These allostratigraphic units possess different ages,
Qao2
Twtr
Twh
Kg
Titd
Qct
Qay
Kclt
Qdsct
Twt
Tgl
1918
Tita
KgTitaQarTitaTitaafe
Tita
Qao2
Qar
Kclt
Tgl
Qsec
Ts
Qao1
Qao1
af
50
52
QarTwtr
18
Tist
Twh Qay
Psf
Kc
Twh
Qao2
Tgjpt
Timd
Qao2 Qay
Twh Qct
Qay
Qao1
Tc
TwhQay
Qayr
Kg
Qao2
Qct
although the sediment looks relatively similar within the overall lithostratigraphic unit (such as in Qao).
Twtt
Qct
Twtr
Qao
Tgjt
18
Qao1
TwtrQct
62 5
40
KcltQay Qse/Kc
Qay
Qao3
16
Tws
29
Qay
Twh Ts
Tsb
Twtt15 Tws
Twtt
Qao2
25
Kg
Tist
61
Kg
Qao2
Timd
60
Twh
12Qao1
21
Kg
Twh
Twtt
Qay
Twh Ts
Ts
Qay
Qse/Kg Kclt Kcaf
Tgjb
Tist
Twh Twtt
Qao2
75
31
Qay QayrTim
Qay
8
Qls Tgjta
Kmd
Qar
Twh
Psf 10
af Kc
Qse/Kc Qay
QseTwh
Twtd
Surface characteristics aid in mapping Quaternary lithostratigraphic and allostratigraphic units. Older deposits generally have older surfaces, so
Qay
Qar Qay
Qao2
Qls
Qtg
31 36
Kmd20Qec
15
Qao2
Tsx
Qay
Qay
13 Kc
47
Qse/Kg
Qay
Twh
Tc
Tim
Qct
27
20
23
Twtt
Qai
18
Twbpt
Qao2 Qay
Qai
Qao2
77
Kg
af
Qay
Qse
Tim
38
Tirt
Qao1
Qao1
af
Kc
Twtr
Qao3
Tgjta
19
Twh
Tc
18
18
surface processes dependent on age — such as desert pavement development, clast varnishing, gypsum and calcium carbonate accumulation, and
Tist
14
Ts
28
8
Kmd Qse Kc
Qar
Twh
Tist
39
Cone Peak Qct
Qse
5 Qls Twh
Qay
Ts
TwhTwh
Twt
Qayr
35
Qao1 Tc
Qao2Twh QayTwtr Qao2Qay Twtt
Qayr Tsx
5
Qay
Twh
Tirt
Qay
Qao2
Kc
KcltQao1
15
Tirt
20
Tc
Kmd
eradication of original bar-and-swale topography — can be used to differentiate the alluvial fan deposits. Locally, erosion may create a young
Qay
Qls
Twh
Twh
Qe
Qar
Qao1
Kg
Twh
Qay
Qls
Qay
Kc
85
Qay Twh
Twh Qay Twtt
Tist
Ts
Qay Qayr
Qao3
9Kmd
Kg Kclt
Qao2
Qao2
Qay
Tws
Kc
Tgjpt
11
15
Ts
Tim
Qay
Qay
Tsx
Qayr
surface on top of an older deposit, so care must be exercised in using surface characteristics to map Quaternary deposits.
Kg
Twtt
Kt
Tist
Tsb
Qao2 Qay Qar Qay Tgl
Qao2 Qse
Qay
Qao1
Kc
Qao1
Twh 28
19
Qsec
16
Kmd7126 Kclt
Qay Qao2
Qao2
80
40
41
Qay
Kc af Qay
Tirt
Qayr
33
Qay
Kclt
Kg
Kc
Kc
Tirt
Twtt
Qao2
Qao2
Twtt
Qay
Kc Qar Qao1
Tgjpt
21
Qse
Qay
Tgl
Qar
15
Qao2
1575Qao Twt
Twh Twtt
Qls
Qao2
Ts
Tgjpt
Kg Qar
Qay
8
15
Kclt
af
Qay
TwhQao2
Tws
Qao1Qar
Qao2Qay
70 Tsts
Qar
22
Qao
Twtt
Qao2
Tgl Tc
Twtr
QUATERNARY–PLIOCENE SEDIMENTARY UNITS
Qao2Ts
Qao2 Kmd Tim
Qay
60
Tist Qtg
Tgjta
Twh
15
Tirt
Qao2
Qao2
Qar
53
Twh
Ts
Qao
Qao1
Qao2
Qay
TwhQao2 Twtt
Qay
Twtr
Qct
Qct Twtt
Qao2
55
Qayr
Ts Twh
Qar Qao Qao2
Qay
Tgjb
Twtt
Qay
Kmd
Twh
Qao2
40
38
Tirt
Twbpt
Tirt
Twh
Qay
7
11
Twbpt Tgl
4
Qao2 Twh
Twh
70
Tsts
Kmd
Qayr
Tgjpt Tgjt
af Qar
Qay
Qao2Qao2
Qay
Qct Tita
Qao2
Timp
Qar
Tc 44
Twh Qay
Tirt
Qao2Qao1
Twtr
Qao2
18
Twbpt
ARTIFICIAL FILL AND EXCAVATIONS
Qao2
Tgl TglTgl
TwhTwh
20Twtr
Qao2 Qao2
18
Twt
Tgjpt
Twh
Qay
Qec
Twtr Qayr Twtr
Tist
Twtr
KtKmd
10
Twh
Twh
Twtt
Qay
Qay
Qao2
Qao2
af
Twtt
Qse
Twtr
Twtr
Qao2 Qao2
Qse
Qay
Tgjpt Tgjpt Tgjpt
Qao
Kt 84
Twtr
Tc 52
Kg Qar
Timp
12
Twh
Tgl
Qls
Qai
Kc
Qe
3
Twh
Qay
Qao2
Qay
5
Qao2
Kc
Qai
Twbpt
Twtt
Twtd
Tist
Tgjta
TwtrQseTwtt
Qay 74 15
Qec
Qao2
Qar Tgl
Tsx
Qayr
2517
Qao2
Twtt
Qsec
TwhQse
Qao2
TwhQai 30 TwhTwh
Titd Twh
Qay Qao2
Tc
Twtt
Timp
1015 Qao2
Qay
Twt
Qao2
Kc
Qai Qls
Twtt
Kmd
Kg
Kg
Twtr
Artificial fill (modern)—Compacted silt, clay, and sand (minor pebbles) under highways and railroads. In the case of railroads, coarse to very
3
Tgl
Tita
Qay
Tgl 22
Qao2
af
Twh QseQse
Qay
25
Timp
Tgl Tgjta Tgjpt
Qayr
Qao2
Twh
Qao2Qao2Kmd
Tita
Qao2
Qao2
Qay
Qay
55
Twt
Qao2
Tc
Qay
Qct
Tc
Twtt
Tita
Tgjpt
50Qao2
Twtt
Twh
Twtt
Qao2
Qao2
Tc
Twtt
Twbpt
Qse
Qao2
Qay
Tgl
Qls
Qayr
Qay Qar
Qse/Kg
65
Tgl
Tita
Timd
Qls
Qay QseQay
coarse pebbles and fine cobbles drape compacted fill.
KgTimp
QayQao2
Qay
Qay
Twbpt
Tgl
Qao2
Qao2
Tgl
10
Qse
Kg
Timd
Qay
Tirt
Tita
Tirt
Qct
10
Qay
Twbpt Tgl Tgl
Qao2 Qao2 Qao2
Qao2
Qay
Tgjb
Qay
Qao2
Twtt
Qao2
Qar
TcTc
7
Qao2
Twt
Qao2 Kg
30
Tsts
Qayr
7
Tgjt
af
Tgl
Tgjta
af
Tigjb
Qao2
Twh Qse
Tita
qv
Tgl
Qse
Qayr
Tgjt
Qay
8
Qao2
30
Tgl
Qay
Qay
Timd
Tgjt
Twbpt
Qct
Tgjbt
Tgjta
Tgjta
Tita
Twbpt
TgjtaTigjb
Qec
Qayr
Kd^m
Tgl
Tgjpt
Qao2
Qay
42Tist
Ts
45
Qao2 Qec Qay
TigjbTgl 9
Tgjpt Tgjb
Twt
HILLSLOPE AND MASS-WASTING DEPOSITS
Qay
23
Qao3
Twt
Qay
Qec Qao2
Qay
Pag
Tgjt 60
Qec
13
Qec
Tc
Titd
Qay
Tgjpt
Tgjbt
Qse
Qay
Tc
Tc
Tid
Ts
20
qv
Twtr
Qay
Tgl
Qao3
Tist
Py
15
45
Tstg
3
Qao2
Qay
10
Qse
Ts
Psf
Tc
Twt
28
13
Qec Qec
Qayr
Qay
Py
Py
Qay
Qao2
Twh
Tgjpt
Tist
45
Qay
5
Qao2
Qao2
Qay
Colluvium and talus (middle to upper Pleistocene and Holocene)—Angular gravel and sand deposited on or adjacent to steep slopes. Sediment
Qec
Tid
Qao
7
Tc
Qct
Qao2
Qao2
Qao2
Qct
Qct16
Qay
Twt
Tita
Qayr
Ts
7
Qay
Qar
Tgjpt
10
42
Qao2
Qct
Qay
45
Qay
13
Twt
11
Tgl
Qay
33°25'0"N Py
Qay
Qay
lacks distinctive bedding and is very poorly sorted. Gravel consists of pebbles, cobbles, and boulders. Matrix consists of sand, minor clay–silt, and
20
4
Tgjb
52Kc 30
12
Tgjta
Qay
^m
Qec
af
Qao2
Twt
Tgl
Tstg
Qao2
5
Tgl
Timd
Qec
Qay
19
Qao2 Qao2
Qsec
4
Qay Qec
Qao2
10
Qao2
Twtt
Tgjpt
Qec
85
is notably gypsiferous to the south. Weak to absent soil development. 1–6(?) m thick.
Tgjta
40
Qse
Qay
Twtt
Qao2
Py
Qao2 Psr
Tc
Kc Qay
Tist
Qayr
QeQe
33°25'0"N
Qec
Qct Tist
Qao
72
Kd
Tstg
29
Tid Timp
Qdsct
Qay Qay
Qayr
Twt
Qay
Qao2
Tstg
Tgjpt
Qse
Qsec
Qao2
70
45 Tim
Qao2
50
Qayr
Qay
^m
Kc
Qdsct
Qay
Tgjb
7
Tist
Qay af Qay
Qay
Qayr
Tist
Qec
Qao2
Tist
Qay
Tist
Tist
80
5
Kc Tim
^m
Tid
TglTist
Qay
Qao
Psr
Titb
Timp
Kc
Landslide deposits (upper to middle Pleistocene)—Two types of landslide deposits are present: 1) weakly consolidated, very poorly sorted, anguQayr Qay Qao2
Qay
af Qay af
Qao1 Tist
Qar
Tgl
Qdsct
Twh Qar
30Qe
Qls
Qao2
Qec
Titb
7
5
Qse
Qse/Psf Qse Qao2
Qao2
Qao2
55
Qec
Qao2
70
Titb
Qdsct
Tist
Qay
Qay
Qao2
Qec
Qao1
Tsts
Qec
Tgjta
Qay
Tid
lar cobbles and boulders (minor pebbles) in a light brown matrix of very fine- to fine-grained sand (5–10% silt–clay) and minor coarser sand, up
Twt
Twtt
5
Qao2
Tgl
^m
Qao2
10
16 Titb
Qay
Tgjvs
Qed
Tirt
Qao2
Twh
QayPsf
5
55
Qct
Qayr
Qay
Titb
Qao2
Qdsct
32 Qar
Twh
47
Tirt
19
to 60 m thick; 2) large, semi-cohesive blocks derived from uphill escarpments of competent rock, 1–6 m thick.
Qed Psf
15
Tgl
Qay
Qar
Qao2
Titb
8
Tgl
Kc Titb
Tist
11
Qsec
Twt
Qar
QayQao2
Twt
Qay Qed
Qec Qao2 Qdsct
20
12
Tgjpt
Titb Kc
Titb
Kc Titb
Qao2
Tgjvs
Ts Ts Qay
6
Kc
Qct
Qct
Qay
25
Kc
Qay
Twt
8 12 Qao2
Tist
35
Twt
Qao2
85
Titb
Twt
24
Qay
Qao2 Psf
KcTitb
Qao2
Qao2
Qao2
Tgjvs Tgjvs
Twt
Qayr
Qao2
Qay
Titb
Qay
7
Tgjvs
Kc
Titb
Tist
Qed
Qse
Kc
35 Titd
Qao2
70
af
Qao2
Qse
Tstg
Twt
Qay
Qdsct Debris flows, slopewash, colluvium, and talus on steep hillslopes (upper Pleistocene to Holocene)—Gravelly sediment on steep slopes inferred
Kc
Qao2
27
Qay
Ts
50
Qai
Qay
QTg
Qay
Qay
Titb
Qao
17
Qao2
Qao1
Qao1
Qed
75
Twtt 42
Titb
Qed Qed
Kc
Titb
Twtt
QayQay
Qay
Qct
Qse Qao2
Twh Twt
Twt
6
Ts
Qai
to have been deposited by debris flows or processes associated with colluvium or talus. Commonly matrix-supported. Gravel is angular and mostly
Qec
Tc
Qao2
Titb
Kd 5
Qayr
Qao
Qay
Qay
QayrQayr
Twt
Tsts
Qay Qay
Qao2
QayQay
2
Twtt
Tc
QarQay
Qec
Twtt
Qao2
Twh
Qtg
Tgjta Qse
Qao1 Qao1 Qay Qay
15
Qao2 Qay
5 145 Kc12
Kc
Titb
Qay Qay
Qct
Titb
Qct
18
204Qay
consists of medium to very coarse pebbles and cobbles, but includes minor finer pebbles and boulders. Unit is commonly overlain by finer-grained
Qao2
Twbpt
Kc
Psf
Qec
Qay
Qay
11
11
35
Qar
Qay
Qct
Tgl
Titb382 5 17
Qao1
Qao2 Qao2
Twt
Qar
Qay
Qed Qec
Qao2
Qay
Qtg
Qe
Qed Qed
30
Tc
70
5
Tstg
70
Qct Qao2 QTg
Qay
slopewash deposits of clayey-silty, gravelly sand. Weakly to non consolidated. 1–10(?) m thick.
Qct
6 Qe
Qdsct Tgjpt
Qay
Qay
Qao2
25
Qay
Qed
Qec Qay
Qao2
Kc
Qay
Titb Titb
23
Twt
Qed
Qay
Qao1 Qay
Psf Qse Qay Qao
Qao2
Qao2
QTg
Qse
7 10Titb
Kc
QeQao2 ^m
KdKd
Qay
Qao1
Qao2
Qay
15
Qec Qay
Kc
Kc
Timp
Qay Qay
Kc
Qao2
27
Tc
Qay
Tsts
QseQay
Qao2
10
Qar 6
27 31
Titb
35 30
Qay
Qao2Qay
29
85
Qay
Twt
Qao1
Qe
Qar
Qct
Kc
QTg
EOLIAN AND SHEETFLOOD–SLOPEWASH DEPOSITS
10
28 Qao2
Twt
Qao QsecQay
Qayr
Qse
Qed
7
Twtt Kc
Qay Kc
Psr Psr Qe
QeQeQe QeQao2
Qayr
Qay
20
Qay
Twbpt
7
Qse
Qao2
Titb
Tc15
Qay
Kt
18
Ts
Twt
Qay
Qct
10
7 Qay
43
Tsts
Qar
Twtr
Titb
Tim
Qay
Titb
Qec
Kc
Titb
Tirt
Qao1
Qec
Qay
Qao2
Titb 10 Titb
10
Tgjta
Kc
Qay
Kml
Qay
Qay
15
Qao2 55
Qct
Qao1
Tgjb
Kt
Qay Qe 66
Qct
Qay
Qse/Psf
Qar
50
Twtt
Qayr
50
Kc
Kc
Eolian sand deposits, undivided (middle to upper Holocene—Undivided eolian sand that is mostly brown to light brown, very fine- to mediQao1 40
Qao2 Kt
Titb
Qe
3
15
Qse
^m
Qed
Qao2
Qay
Qec
Qao1
Qay
Qao2
Qse/PsfQse
4 5
65
6
Kml
Qay
Kd
Qar
25
Tc
75
3
Qec
Tgjb
Qed
um-grained (minor coarser sand). Includes eolian sand ramps that slope away from topographic highs. Loose and several meters thick.
38
Qar
Tgjpt
5
Qec
Qay
Tgjvs
Qct
Tc
Qar
Kc Qay
Qao2
Tsts
Qayr
Qse/Psf
Qao1Twh
Qao
12
Qao2
Qec
Qec Qct
Qar
5
Qao2
Qao1
Qay
Qsec
Qe
9
31
Qao1
Qao2
Qay
Qar
Qay
Twtt
21
Qay
Qed
Tgl
Twt
Qao2
Qay
QecQao
af
Qay Qe 34 Qay
Qay
Qai Qay
Twh Qao
Qay
Tgjta
Qao1
Qay Qse/Psf
Qao2
Qao2
Twh
17
QecQay Tita
Qao2
Qse
Qao2
Qec Coppice dunes (upper Holocene)—Mounds of brown sand accumulated around shrubs, where dunes exceed 5% surface cover. Mounds range
Qec
Qay
Qec
Psf
Twt
Qayr
Kc
25
37
Tstg
Qdsct
Qay Qao2
Tgjta
12
Qmo
Psr
Kc
Qay
Qec
10
Qec
Qay
Twh
Tc
Timd
from 10–200 cm in height. Sand is very fine- to medium-grained (mostly fine-grained), with 1–5% coarse to very coarse, scattered sand grains.
Qao2
Qao2
Qay
Qct
Qay
Kc
^m
Twh
Qse/Psf
Tim
Qao2 Tgjpt
Qct
Qtr Qay
Qay
Qao2
6 7
Qao2
8618Qao
Qay Qay
Tstg
Qayr
Kd
Tc
Qao2
Coppice dunes overlie a bioturbated eolian sand sheet or sheetflood deposits (with a sparse pebble lag). Loose. Deposit under the dunes is up
8
Tgl
Qar
Qec
Qao2
Qao2
83
70
Qec QsecQct Qay
Qao2 Qao2
Qayr
Qay Qay
Qay
Qmo
Twt
Qec
Qayr Qao1 Tgl 22
Qao
Qay
Qao 22 3
Qay
18
Twt
10
33
Qec
Qao1
to ~2 m thick. Unit includes coppice dunes developed on sand ramps, where the entire eolian deposit may be several meters thick.
Qct
Qsec/Qay
Qec Qao2
Qao2
13
Qay
Twtt
Twh
Qse
Qao1
Qayr
af
Qmo
Qay
Qao 77
Qsec/Qay
Tc
Kc Qar
25
68
Qsc/Qao2
Qar
12
19
Qao2
Qar
Qdsct
Qay QayQay
Qay Qay
Tifg
Qsec/Qay
QTg
Qay
Qay
Qay
Tc
Ts
46
Qec
Kc
Qar
Qao
Tgjb
Qao2
Tgl
Qao2
44
Qao2 Qayr
Qay
Qai
Qay
Tgjpt
Qay
Qao2
KcQe
Qsc/Qao2
Tifg Tifg
Qay
Qao
Qao1 Qayr
Qct
Qec
Qao2 Qayr
Twh
Qao1
Qec
Qao2
69
Qec
Qay
Tgjpt TgjbTgjb Tgjta
Qao1
Qao1
Qed Eolian sand in dune forms other than coppice dunes (middle to upper Holocene)—Eolian sand in mound-like deposits that extend over several
Qdsct
Qao1 Qar
Qao2
QayrQao
Qec Qec
33°22'30"N
Qayr
Tgl
Twtr
Qay
Qay
68
Qec
Qay
Qsec/Qao2
Tgjta
Qay
Qay
Qec
Qec
af
Qayr
Qec
Qay
Qec
Qay
Qay
Qec Qay
Twbpt
Qao2
Qayr
Qay
Qao
Qsec Qay
Qec Qec
Qay
Qao2
Qec
Psh
Qao1
Tgjpt
Qao1
Qec
Qar
Qao1
Tifg
Qct
Qao1
Qay
Qec
Qao1
Tc
Qay
Qao2
Qao1
Qay
Qayr
TwhTid
meters. Dunes are 30–100 cm tall, commonly elongated NE–SW (3–30 m in length), and overlie sheetflood deposits or eolian sand sheets correlQay
Qao1
Tglta
Qayr
Qay
Tgjpt
Tc 48
Kc
Tc
Qao
Qao1
Qay
Qao1
Qao1
Qay
Qec
Tglta
Qct
Qec
Tgl
Qayr
Tglta
Qsec/Qao2
Qao1
Twtr
6
Qmo
Tifg
Qar afe
Qao
Qao1
Qdsct Tglta
Qay
Qao2
Qao1
Qao
Qar Qao2 Qao1 Qao1
Qao1
Qao Qao1 Qay
afe
Tgjvs
QayQao2Qai Qay
Qay
Qao1 Kc Qayr
Tgl
Qary
Qayr
33°22'30"N
Twtr
Qay Qay Qec
Qct
Tglta
QaoQao1
Tgl
105°55'0"W
Qao2
ative to Qse (included with this unit). Sand is light brown to reddish-yellow and fine- to medium-grained. Loose and up to 3 m thick.
Qec
Qe Qay Qec
Tgl
Qay
Qao1
Tgjpt
105°52'30"W
Qai
Qayr
^m
Qed
105°50'0"W
Qdsct
Qay Kc
Tgjb
Qao2 Qay
105°47'30"W
9
Qay
Psr
Qao2 Qao1 Qao1 QayQar Qay Qao2 Qao QayTglta
Qay
Kd
Qe
Qse
Qe
Qay
Qe
Qay
Qay
Tgjvs
Qay
Tim
Psf
Tgjta
Qay Qao2
Tim Km
Qay
Qay
Qay
Kml
Qec Qay
QayQayr
Qay
Qao2Qar
Qay2 Qay
Qay
TgjbTglta
Km
Qay Qay Tim Tglta
Qao
Tglta
Qay
Qec
Qec
Tim Km TimTim
28Qay Qsec/Qao2
Tim
Qay
Qao1
Tglta Tgjpt
QayQao1
20
Qay
Qayr
Qar Qay
Tgjpt Qct
Qse Sheetflood and slopewash deposits, commonly reworking eolian sand sheets (middle to upper Holocene)—Light brown to brown to reddish
Qay
Kc25
Qay
Qayr
Qayr
Kc
Qar
Qao
Qao2
Tglta
Qar
Qao1
Qao2
Qao1
Qao2
Qay
Tglta
yellow, very fine- to medium-grained sand (minor coarser-grained sand). May be composed of pale brown, clayey–silty, very fine- to fine-grained
Qay
afe
QaoQao Qay
24
Qao2
Qao2
Tgl
Qar
Qar Qec
Tgjpt
Qar
Qec Qao2
Qec
Qao2
28
Qay Qsec/Qao2
Qao
Tglta
Qay
QayQar
Kml
QayQayrQayr
Qao1
Qay
Kml
Qay
Tglta
Qay
Qao2
afe
sand at the base of steep slopes. Both deposits contain minor (1–5%), scattered, very fine to coarse pebbles. A very thin pebble bed may be
Tglta
Qao2
Qay
Tglta
Qay
Qay2
Tim
Tglta
Tim
QaoQao1
Qsec/Qao2 Qse/Psf
QayQay
afe
QayTim
Qao1
Kg
Qay
Qao2Qao
Qay
Qao2
Qao2
Tim
Tglta Qct
Qao2
Qao1
Qay2
Qao2
Qed
Qe
Qao1
Qao2
present at base of deposit. Internally massive with weak cumulic soil development characterized by ped development and minor gypsum accumuTim
Qay
Qao
Psf
Tglta
Tid
Tim
Tim
Qec
Kc
Qec
Qao2
Qay
Qay
Tim
Qao2
6
afe
QarQao
Kc
Kg
Qao2
Tim
Qary
QUADRANGLE
LOCATION
Qay
Tim
lation. Local, very thin to thin sandy pebble lenses. Unit locally grades laterally into Qay. Surface commonly has a sparse lag gravel and no to
Qec
Qao2
Qao2
Qe
Qao2
Tim Kg
Tim
Kc
Qao1
Qec
Qay
Tim
Qay
Qay
Qay
Qec
Qay Qao2
Kml Qec
Qedafe
BROKEN
Qao1
Qsec
LITTLE
Qay
Qar
WHITE
weak desert pavement development. Loose to moderately consolidated. 0.2–3 m thick.
PINK
Tita
Qay
Qar
LONE
Km
Kg Tim
Qao2
BACK CRATER
Qay
BLACK PEAK
OAKS NORTH
PEAK
Qay
Qay
MOUNTAIN
Kg 13
Qay2
Qec Tim
afe
Qao1 Qao2
Qar
Qay
Qsec
Qsec/Qao2
Qay
Tim
1.5
0.75
0
1.5 MILE
Qao2
Tim Qar
Qao2
Qay Qec
Twh
60 Tim Qay
Qay
Kc
Qar Twh
Qar Tim
Timp
Qao3
afe
Qse/Tc Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the Cub Mountain FormaQay
Qar
Kclt
Kc
Twh
Qe
65
KcKc
60
Qao3
Qsec/Qao2
Qec
Qe
Qec
Qay
afe Qay
tion—See descriptions for units Qse (above) and Tc (below),
WHITE
Qay
Qao2
Qec
Tim
RED
WAGON
Twh
CARRIZOZO
CARRIZOZO
18 Tim
Qay
Qay
Qec Qao2
Twh
21Tim
OAKS
Qsec/Qao2
CANYON
Qary
CANYON
WEST
EAST
New
Mexico
1000 0 1000 2000 3000 4000 5000 6000 7000 FEET
Qar Qec Tim Tim
Kc17
Qayr
Qec
SOUTH
40
Qao2
Qao2
Tim
Kg
Tim
Qse
Qsec Ts
Qay
Qe
Qsec
Qsec
Qse
Qao2
Qay2
Qay
Qay Qay
Qao2
3 Rivers
Qar
Qec
Qsec
Qse/Kc Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the Crevasse Canyon
Qec
Qar
Tc 45
afe
Qao3
Qse
Tim
Qay Qec Qay Qar Qay
Qe
Qse/Kc
Kc
Qse/Kc
Sand
well
1
0.5
0
1 KILOMETER
Qec
Qse/Kg
Qec
Qar
Tc
Qay2
Qsec
Qse/Kc
afe
Qec
Formation—See descriptions for units Qse (above) and Kc (below).
Qao2
Qse
Qay
Qay2
Qay/Qai
Qao2
Kc
Qec
3
Rivers
Petroglyph
Qay2
(TB-155)
Qec
Qayr
Qay2
Qay
Tim
Qao2
Twh Twh
Qec
BLM campground
Qay2
Qayr
Kc
Tim
Timp
Qao2
Qao2
Qse
Kg
Qao2
Kc
Tim
Tim
Qec
(TB-019) 27
Qao
Qar
Qct Twh
Qar
BULL
afeafe
Qec Qsec/QayQay
Qay
Qao2
CUB
Qay
Tim
CHURCH
Qec
Qse/Kg Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the Gallup Sandstone—See
Qao
BULL GAP
Qao2
NOGAL
CONTOUR INTERVAL VARIES
Qay
GAP SW
Magnetic Declination
Qay
Qar
Qar
MOUNTAIN
MOUNTAIN
Qai
Qao2
3 Rivers
Twh
Tim
Qay
Qao2
descriptions for units Qse (above) and Kg (below).
3
Rivers
Qao1
Qsec/Qao2
June 2012
Qay
Qec
BLM well
Qar
Qao1
NATIONAL GEODETIC VERTICAL DATUM OF 1929
Tc
Qay
Qar
fee well
Qao1
Qar
Twh
Qay
8º
36'
East
Qay
(TB-062)
Qao2
Qay
Qary
Qay2
Qay
(TB-244)
Qao2
afe Qar
afe Qar
Tc
At Map Center
Qao2
Qe
Qao2
Qao2
Qay
Qay
afe Qay
Qse/Kmd Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the D-Cross Member of the
Qay/Qai
Qse
Qay
Qe
afe afe
3Qec
Rivers
Qay
Qay
Qe
Qao2
Qay
Mancos Shale—See descriptions for units Qse (above) and Kmd (below).
afe
Qay
Qec Qse
Qao2
Qao1
Qao2
Qay
Qe
runway well
Qay
Qay
Qse
Qec
Kc QayQay
Qao2
THREE
GODFREY
NOGAL
Qao1
Qay
OSCURA
ANGUS
(TB-061_
afe
RIVERS NW
PEAK
Qary
PEAK
3 Rivers
3 Rivers Headquarters
Qec
Qao
Qay
QayQay
Kc KcQse Qar
Qec
33°20'0"N
Qay
Kc Qary
Qse/Qao2
Qay
Kc
IrrigationafeHeadquarters House
TimKc Qse
Qtg
Qse/Psf Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the Four Mile Draw Member
Qe
34
QtgQtg
Qtg
Tita
Qtg
33°20'0"N
Qay
Qtg
Kc
Qay
Qao3
Kc
Qse/Qao2
well (TB-059) well (TB-060)
Qtg
Tim
Kc Tc
28 Qay
Qao2
Qay
of the San Andres Formation—See descriptions for units Qse (above) and Kmd (below).
38
Twh
Qtg
Qay
Qay
3
Rivers
25
Kc
Kc Qse Qay Tid
Qtg
Qtg
QayTc Qay Kc 4
Qao1
Qtg
Qay
Qay
Tim
Qe
Qary
TcQary Tc
Kc
Qary Tim
Qao1
Qec
QaoQao Qtg Qtg GatehouseQay
KcQtg
Qary
Kc
Twh
Titd
Tim
Qay
25
7
Qec
Qary
Qay
Kc
32
Qay
Qao
Tid
afe
Qay
Tc
Tim
16Twh
Qay
Tid
Tc
Qay
Qse
well (TB-058)
Titd Titd
Qay
TcQay
23 Kc Tim
Qay
4
27 20 Qay
Qtg
14
5 Kc
Tc Tim
Qao3 QayQay Qsec
Qay
Titd
Qary
Tita
Qay Qec
Qao
8 Kc Tim
Qay
Kc Kc
Tc
Qao
Qay
Qao2
585
Qary
KcTim
Qsec Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, with coppice dunes on the surface
16
Qao2 Qary
5 Qary50Kc
Titb
Qsec/Qay
Qay
SIERRA
Qec
Qao2 Tim
Qao
THREE
Qse
THREE
GOLONDRINA
Qse
Kc
Qec Qao3
Kc
Qtg
Qec
Qse
BLANCA
QTg
RUIDOSO
Qec
Qay
20
(middle to upper Holocene)—Similar to unit Qse, but with 5% or greater surface coverage by coppice dunes. See descriptions of Qse and Qec
Qec
Kd QtgQse
RIVERS SW
RIVERS
DRAW
Titb
Tc
Qec Qao Qao
Kc
Kc
Qay Qay
PEAK
10
Tim 8 Qao1
Qao2
Titd
Tim
Kc
Tid KcTita
Qary
Kc Tim
Kc
425 4
Kc
Qtg Qao3 Qao1
Tc
Tim
Qao
Tc
afe
Qec
Qtg Kclt
(above).
Qse
Titd
10
14
Qao3
Tc
Kc
Tim
Qao
11
Qse
Tim
Kc
afe10 Kd Qtg
Tid 3
TitdKc
Kc40 Qay/Qai
QaoQao Qtg
Qao2
37
Qtg
Qay
10
Kc
Qtg Kd 9 ^m
TcTc
TitbTim
Qe
TitdKclt Qtg
Qay
Qao2
Kd
Qay
^m
Qao2
Qao3
Qay
Kc
Tbf
Qay/Qai
Tim
Kc
Qao2
3 Rivers
Tc Tc
Tita Kc
Kg16
Qay
Qay
Qay Kc 2727
28 13
TcTita
Qay
CAT
APACHE
Qao2 Qao2 Qao2
BITTER
Qao2
18 Qao2 QseKc Qary
Qe Qe
KcQary
TULAROSA NE
Tim QTg
Qao2
Qao2 Qay Kg 8 Kclt Qao1
Tc Qao2Qay
13
Qao2
Kd
Kc 10 Tim
MESCALERO
Tim
Rivers ^m
Qary 42
Kc
Qao2Qao2
Qao2
Tim
2224
Tim
Kc Qay Kc
Qay afe
MOUNTAIN
SUMMIT
Tc
CREEK
Railroad
Well 3 Qao2
Qao2
Kc
Qtg Qao2
Qsec/Qay Sheetflood–slopewash deposits and coppice dunes, undivided, overlying younger alluvium—See descriptions for units Qsec (above) and
Tim
Kc Kc
KgKclt
Qao2
^m
Qary
Tim
Titd
Tim
Kc
Titb
Tim
Kclt
Kg
Qtg
3
Qar
Qao2
Qao2
Qay
Qtg
Qao2
Qe
Qao
Qao2
Titb
Railroad
Well
Qao2
afe
Kc
Qay
Qao2
Tim
12
Qay
Qse
Qtg
#1 (TB-057)
Qse
Kc
Kg
Km
10
Tim
Pag
Qary
15
Qec
Kd
Kd
Qay (below).
Qtg
Qtg
Qary
Qao1
Kc Qao2
Qec
Tc
Qar 32
^m
Tim
Pag
Qay
#2
(TB-056)
Qse
Pag
Qary
Qao2 QtgQao1 Qtg Km
10 Kc
Qao2Qao2 Qtg
Timp Qao1 30
Tc
Qe
22
Kc
Qay
^m
Kc Kc Tim
Qay
Qary
Qao2
Qao2
Kd
Qary
Qtg
Qao2
Qao2
Kc
Qao2
Kclt
Qtg
Qayr
Qao
Qao2
Tc Tid
Qao1 Tbf
Qary Kc
Tim
Tim
Kd Qao2
Kclt
Qar
Kc
Qao Qay Qao2
Kg
Qao1
Qao2 Qse
21
Qao1
Qao1
Kclt
Qar
TimKc
QayQay
Qao2 Kd
Tita
Qao1
Qao2
21
58
13Tbf Qao1
Kc 35
Qao 25
Qsec/Qao2 Sheetflood–slopewash deposits and coppice dunes, undivided, overlying the middle subunit of older alluvium—See descriptions for units
Qay
afe
Qay
Qao2 Qao Qay
Qao2
Kclt
Qao1
Qao2
Tbf
Tc
Qao2
Qay Titd Qay
QayQary
Qay Qao2
Qao2
Qao1
Qao
Qao2
Kc
Tc
Tim
Kclt
Tita
Pag
Tbf
Kc
Qao
Qsec (above) and Qao2 (below).
Qay
Tim
Qay
Qao2
Kd
Kml
Qao2
Qay
Qay
Qary
Qay
Qao2
Kc
Kc
Tim
Kg
Qay
46Qao 10 Qse
Kc
29Qar Qao2 Qao
^m Titd
Qao Qao1
Qary
Qay
Pag
Qay
TcQay
Tita
afe Qayr
Qay
Qao2
Qay Tim
28
Kc
Qao2
Qao2
Qay
Kc
KcQao2
Qao2
TiTc
Qay
Qao2
Tid
Qay
Tc
Qse
24
22
Tc
Tim
Tim
Qao2
QTg
Tim
Qao1
Qay
Qao2
Kc21 Tc
TimQao3 KcKcQayKcQay
Qao2
Qay
Qao2
Qay 23
Qary
Qsec/Qao2 Qay Pag
Tim
Qay
QaoKdQtgQao3
27 Qao2
afe
Qay
Qay Qay
Tim
Qao2
Qay
32Qay27
Qay
Qay
Qary Kc
Qao2
Tid
TimKc
Tim
Kc
Qay
Tita
Qtg Qao Tbf Km Qay 5
Qay
40Qayr
^mQay
Qay Qao
Qao2
TimQary
Tid
PRECIPITATE DEPOSITS
Tim
TidTim
9
Qay
30 Qay
Kc Qao2 Qay Qao2
QseQao2
Kclt
Qao2
Qay
31
Kc
Tim
Ti
32
Qay
Qay
Kg
39
Tid
Qary
Tim
Kc
Qao1
Tim
Kc
Tid
Tid
TidTim Kc
Qao2
^m
QayrQay
Qao2
QtgKm
Qao
Kc
24
Pag
Qao1
10
Qao2
Qao
Qay
QTg
Qao
Kc
30
Kc
54
Qsec
Tim
Tid
Kg 41
Pag
QTg
25
Tid
Tid
Qay
Qay
Qay
Qay
Kc
Tim
Qar
Kc
Qao2
Qay
Kc
Kc
Qay
Tid
Tid
Tid Tid
Qay
Qay
Pag Qtg Kd
Tid
Qay
KcTid
Qay
Niccum
Tid
Tid Tid
QTg
Qct Qay
Qtg
Qao2 TimKclt Qao1
Qay
Pag
Kclt
Qay
Kg
TidQao1
^m
Kclt
Kc
12 Tid
Kclt
Qar
Qay Kc
Qtg
Kg Tim
Qtg
33 Tid
well
5
Tim 50
70Qay
Qgy Gypsum at the base of steep slopes west of Oscura (upper Pleistocene to Holocene)—Gypsum in a tabular layer or possibly in an eolian sand
Qtg
22
Qay
Qao2
Qct QtgQao1
Tita
QTg
Kg
Qao1
Kc
Qao2
Kc
Qse
27
27
Qary
Kc
Kc
TB-030
Kg
Kg Kclt
Qao
Tim
Qao
Qao2
Qao2
Qtg
sheet. Inferred to have been deposited by wind and then later experienced dissolution–precipitation events. 1 m thick?
Tid
Qao1
Qao1
Qao2
Qao2
Tim
Kt
Kc
Kc
Kc
Tita
Kc
Tita
Qct
3
7
Km
24 KtKt
34
Tid
QayKcltQao2
Tid Kc Kc
Qct
Kg Qao1
Qay
Qao2
Tita
Qay
7
Km
Kt
QayQao Kg
Kc
Qao1Km
Kml
Kclt
Tid
QseQao
Tita
30
Tita
QTg
Km
Qay
32 Qct Tid
Tita Tita
37
Qay
8
State
Qao2
Qao2 Qao
afe
Qao1
Tita
Qary
Qao1
Tim
Qay Qao2
Travertine (middle to upper Pleistocene?)—Thin to medium, tabular beds of gray to tan calcium carbonate near the western quadrangle border.
Qse
23
Qay
Qao1
Kc7 9Kc QTg 10
Qtr
Kml
L.G.
14
NIccum
well
Qay
Qao2
Kclt QTg Kc
5
Qao
Kc
QayQay
Tita
Qar
2
Kml
Qay
10
Kg
"1453"
1A
(TB-026)
Microkarst topography common on the travertine surface. Probably deposited in a series of seeps or springs during paleoclimates with higher
Tita
Qay
Qar
Kg
3
6
Qay
13
afe
Kt
Qao1
710
Qao2
8
Qay
Qay
Tid Qay
4 411Qao2
Qay
TidKml
Qao1
Qay
Qao
Qao2
Qar
Kmd
Qay
precipitation rates than today.
Qay
Qay
Kmd
Qay Qay
QayQay
Qay
Qao2
14
Tim
Qao2 Qay
13
Qay
Qay
QTid
ay
QayQao2
Qao
Lewelling #2
Qay Qay
Lewelling #1 Qay
Qay Qay
Qay
Tid Kclt Qao2
Qao1
Qay
Qay
Qay
9
Qao2
Qao
Qay
Qay
15
Qao2
Qay
Kd
Qay
Kc
12
7
5
Tid
11
Qay
Kt Kmd 77
Tid
Kd
Qay
Qay Qay
Kml
Qao2 Qay
Qay
^m Qls
Qse
Ti Kd Kd
Kml
Qao2
12
Qct
Qct
13Qay
18
Qct
Qao 23
7
Tita
Qse
afe
Qay Qay
Qary
Qct
Qao1
Qay
KtQao
Qao
Qct
Qay
Niccum
Qayr
Quartz veins (Oligocene)—Milky quartz precipitated in veins.
Niccum
Qary
33°17'30"N
Niccum well
9
7
Qao2
Qay Qay
qv
Qay
Pag
Qse
Qao2
2
Qse
Qct
Kt
Qct
Qao1
Qay
Titd
well
2
5
Qay
Qao
well
6
Qay
Kd
Tid
10 (TB-025) Qar
Qao1 Tita
33°17'30"N
Qay
Qar
10
Kclt
Tita
10
QTg
5
11
5
Tim5 9
Kc
Tita
Qay
Qct
Qct 620
(TB-027)
30
1010
Qao2^m
(TB-031)
QTg
afe
Pag
Qao2
Qay
afe
Qay
Kclt Tid
GLACIAL MORAINE AND OUTWASH DEPOSITS
Niccum
KcTitd
Kclt
Titd
7
4
Qse
Kg
Qao
Tid
Qao2 Pag
Tim
Titb Tim
Pag
QctKd Kd
Qar
Tim
Kml Qao1
Kmd
well 3
Qec
12 12 16 9
Qao
Qay
Kclt
Titd
Kclt
Kclt
Qay
Qay
Tim
15
723
(TB-028)
Tim Tim
Qct23Tim
11Qao1 Kml
1410
63
QctKg
1117
^m 23
Niccum Qar
8Kd
TidTim
12
Tim
Qay
Titd
1820
1217 16
Tita
Tim Kd
Tim Tita
Qse
Qmo Moraine and outwash deposits near Sierra Blanca (middle to upper Pleistocene)—Glacial moraine deposits noted by Moore et al. (1988) but
Qao1 Qao1
afe
25
Kml
Kmd
15 80
Qay
Qse6666 Tim
9
Qse
28
Qao1
afe
well 7
Qao
26
TimTim
Qay
Qary
Qao
7 Titd 4
Kg
Qao1Qay
Ts
Kml
Qay
18
11
Kmd
Kml Tim
Kg
Qary
Km Tim
Tim
17
Pag
86
Qao2
Tim
15
Qao
Qayr
Kg
not accessible for description. Outwash deposits consist of very poorly sorted boulders, cobbles, and pebbles of crystalline rocks eroded from the
24
^m
Tim
Qary
Kt
Qay
Qar
15
Qao1
12
13
Qao2
Kd
13
Ts
(TB-032)
Qary
Qary
Qay
9 Kclt
Qar
QTg
Qay
Qao3
afe
Qao1 Qao1
Qao
Qtg
Km Qao3
Titd
^m Kd Qary
79Qar 83
Qao2
Kd
Tim
Tita
Qay Kml
Qay
Qay Qay
Tita
TimTimQao Qar
52328
17 23 Kml Kml
Qao11
Pag
20
Tita 7 10
7 Qtg
afe
Qao3
Qayr
1085 8
Kml
15
Qay
Qar
13
7
Qao3
Tim
10 74
Qao3
KmQao3
Three Rivers stock (Moore et al., 1988).
Qao1
Qtg
Qtg
Qao3
Qao1
Qao3
Kd
Kml
Qao
Qay
25
Qay
Qao1
Kmd
21
^m
afe
^m
37
48
Qay
QctQay24
Qse
Km
24QTg 12
Qay Qao3 Qao3
30Qao3
Tita Titd
Km
Kd
Qao3
Qao2 KgKd
Qao1
Km
Qao1
65 2517 Kmd3022
30 85
Tid
Kt Kml
Km
Qay
Pag
Timp
Kd 6
Km
Qay71
Qct
Tita
48Qse
Tim
Kd
Qao21210
NIccum
Tita
Kml
Tim
Tim
Kd 17
6
Tim
47
18
Tita
20
40
18
8
11 Kml
QTg
Kg 15 Qao1
Kd
^m PagQct10
Qse
Qao1
Psf
Kml Tid
17
7
15 QTg 14Kt Kmd
QTg Tim
Qay
5Kd
KmlTitd Qao2
well 8 Kg Qao2
Tita
Qao1
8
7
Pag
14
Qao
Qay
23
12
10 7 Tid
Pag
ALLUVIAL DEPOSITS
12
17 Kg Kmd
12
^m
Qary
18Kt
Qay
Tita
Qar
afe
Tita
Qay
Qay
Qary
1218Pag
Kmd
30 Kd
Kd
8Kt Qct
26
42 25
8 23
Qao
13
Pag
Tid
Qao
30Pag
Psf
Kml
^m
afe
(TB-033)
Qct
Qao
^m
Tita
Qary Qay
^m
Qao2
Qay
Qay
Qay
Qao
Kd
^m
Tita
^m
Tid
Pag
Tim
17
afe
QaoQao
^m
^m
2717
Qao3
Kml
Qao2Qar Qao Pag
Qao
Kml
KmQao3
Qao1
Tita Kd
QTg
Qary
QayQao1
74
191427
Qao2
^m Qay
Tim
Tid
Km
Titd
Pag
Qay
Tim
Tist
Niccum
Qao
40
Qao3
Qay
Tim
Qct
Qao
Qao1
Qay
Qao
^m
6
4 Kml Qay
Qao
Qao
Pag QTg
^mQao
Qay Qay
QayKd
34
Kd
Pag
Qary Qao1
Kml Tim
Qao2
well 9 Qar afe
Qay
^m
^m Qao2
18
afe
Ti ^m
Qay Qay
Pag
Qao1
^m
Qar Recent alluvium (0–200 years old)—Well-stratified sand and gravel (primarily pebbles and cobbles) in active drainages, where the surface has
13
25
NIccum (TB-024)
Qary Tist14
73
18
Qao1 Qay
Tim
Titd
Qay
Tid
Tid
Tid
Qay
Qao1
Tita
Qao3
Qao
Kd
Qay
Qao
Pag
23
Qary
20
11
Qay
Qay
Titd
Qay
Qao1
Psf
Tita
Tid
Psf
o
well 4
Qao1
l
o
Pag
Qay
e
fresh bar and swale topography up to ~ 60 cm. Also commonly observed as small fan lobes at the mouths of recently incised arroyos, and as a
g
^m Pag Qay
Psf
Qao3
Qay
y an
Qay
Pag Qao1
Qao2
^m 5 TimQao3
Qay Qay
Qay Pag
9
Qay
Qao2Qao
2723
TitdTitdQao1
27
Qao2
Qay
Qao3
Qar
Qayr
Qayr
of G
QaoQay
30 Tita
Qao1
18
Qay Qay
Qayr
(TB-029)
dM
Tid
Qao1
Qao3
Qay
Qay
u
2425
Qsec/Qay
Qay
1
^m
Qay Qary
Qao3
Qao3
25
Qay
Qar
Qse
Qay19
80
^m
Qao1
a
25
Qay
29
Tim
Qay
Qao2
Qay
veneer of laminated sand overlying Qay near active drainages. Occupies shallow valleys in the medial Three Rivers fan, where the sediment is
Qary
Qay
Qao
Qao3
Tim
Tim
e
Kd
Qar TitaTim
Qay
Qao
Tim Qao1 ^m Kd Qct
Qary
Qao1
Qao2
afe
Qao1
56
43
ine
Qary
Tim
15 Qary
Qao3
10Qao2
Qary QarQay
ur
Qse
KdKm Tim
Qay
Kd
Qary
Pag
Qec
B
primarily clay, silt, and very fine- to fine-grained sand. Soil development is very weak to non-existent. 1–3 m thick.
Qay
Qao2
^m
afe
10
Qao2 Tim
Qay
Qao
Qay
Tita
^m
Qao1
2
afe
Kd
Qsp
Tita
Qao2
Km
KdQao2
Pag
Qct
Psf
KmKm
Qay
Tim
Qay
TimKd
Pag
Tim
Qao2 Qay
Km
Qao3
Tist
Tita
Qsec/Qao2
^m
Qao3
Tim
Psf
Tim
Pag
Qay Km Qai
Qsp
Qao2
Titb
^m
7
Qayr Kd
22
Qct
2
Tid
21
Qao3
Kd
Tim
Pag
afe
Kd
Qay
^m
Qai Titb TimTim
Qay
KdQay
Tim
Pag
Qar
QTgQTg Qao3
51Qay
Qct
Kml
Qayr
Qct
^m
Qao
Km
Tim
Tim
Pag
Tist
19 10 TitaPsh
Qao
Qay
QayQay
Km
15
Qct
Qary Recent alluvium, with subordinate younger alluvium (Holocene)—See descriptions for units Qar and Qay. Mapped near modern drainages
Kd
Qao2
14
Tim
10
Kd
^m
Km
Qao2
16
Qay
Qar
Pag
11
Qao3
Pag
Qao2
Qls
^m
Psf
Pag
15
53
Kd
Pag
Tim
11
Tim Km
Qao2
Qay
Qls Pag
Tist 15
Qay
Qls
Qao2
Pag
QTg Qay Qao2
Tid
9 20
Qao3
Qao3
2977Kd
TimQay
Qsec/Qao2
16Qao3
Qay
9
Qao3
Pag
Qao3
Qao1
17
Q
ay
Tim
Pag 11
where Qar and Qay could not be differentiated at this map scale.
Qao2
Qay
Qao2
10
Qay
Qao3
Psr
5
Tim
Titb
Kd
Qary
Pag
Pag
TimKm
Qao2
^m
Qar
^m
23
Qar
Qao2
Qay Pag
75
Qao2Qao2Kd
Qay
Qao1
Qsec/Qay
Pag
Qay
5
^m
afe
38
19
Qao2
Pag
Qse
Qao2
Qao2
Psf
Psf
Qay
Qao1
28
Pag
New Mexico Bureau of Geology and Mineral Resources
Psf 4
Qao2
NEW M EXICO TECH
Qao QTg QTg
15
Psf10Psf 10
Tita
Qao2
Psr
26
Qayr
Qsec/Qay
Km Ti
Qao3
Qec
6
16
QseQao2
Psf
Qay Younger alluvium (lower to upper Holocene)—This lithostratigraphic unit includes three allostratigraphic subunits that were not differentiated at this
Pag
Psf
24
Qct
Qay
Psf
Qse
Tita
Qao2
Qao2
Open File Report 563
Tim
25
Tim
Qao3
Qao3
Qsec/Qay
afe
Qay
9
map scale. The oldest allostratigraphic subunit, mapped adjacent to steep mountain fronts (where it disconformably overlies Qai or Qao), consists
Psf
16
Qct
Qary
16
Qar
QTg
Qao
Qec
Tim
Qao
20
Qayr
Qay Qay
Ea
QTg Qao1
Qao2 Qao2
19
Psh
Kd
7 Psr
19
7
afe
Qao1 Psf Qay Qay
Ti
Qay
Qao1
12
y
Qse
of brown pebbles and sands that are well-stratified to massive and typically fine upwards. Its topsoil is characterized by weak clay illuviation
Kd
10
r
Pag
Qay
Kd
r
Qao2
Tita
Qao2
Qec
Tim
16
th
Qao3 Qay
Mapping of this quadrangle was funded by a matching-funds grant from the STATEMAP program
Qao2
Qao
tu
18
5
Psf
Qay
Qayr
Qao
104
Qao
Qao1
3 4Km
Qay Psf Psf
Qao1
S c ie
Qao
Qao3 Qao2
Qao
Qao
Qao1
en
QarPsfQao1 Qao2
textures and a Stage II to II+ carbonate morphology underlain by Stage I gypsum accumulations.
Qao3
C
Qao3
Qao2
Qay
Pag
Psr
Qay
Qao1
t
of
the
National
Cooperative
Geologic
Mapping
Act,
administered
by
the
U.S.
Geological
Survey,
10
n
Qao2
s
8 1559^m
ce for the 21
Psf
afe
Qay
Qao
29
Qay
Qao2 QTg
Qao2
10 45
Psf
9 15
Qary
Qec
11 10 Qay
77 QaoQao2
Qao
Qay
Qao2
PsfQse Qao1 Kd616 Pag
Qao2
and
by
the
New
Mexico
Bureau
of
Geology
and
Mineral
Resources
(Dr.
Peter
A.
Scholle,
Director
Psf
Qay
Psf
Pag
Qao2
Qay
Qar
Qao Qao1 Qao
35
Qay
Psr
afe
Qay
Pag
3
Tid
Qse
33°15'0"N
afe
Psr
Pag
Qse
Qay Qao2 PsfQao1Qao2Qay
Qao
Pag
Qay
QseQao1
14
Tid
Psf
Pag
Qao1 Qse
11 Qse
Qay
Psf
Psf
and State Geologist, Dr. J. Michael Timmons, Geologic Mapping Program Director).
The second-oldest allostratigraphic unit is the most laterally extensive and locally inset into the oldest allostratigraphic unit. It commonly is brownQao1
Qao1 Recent alluvium, with subordinate younger alluvium (Holocene)—See descriptions for units Qar and Qay. Mapped near modern drainages
? ? Younger
? (lower
? to upper Holocene)—This lithostratigraphic unit includes three allostratigraphic subunits that were not differentiated at this
? ?alluvium
break and scale change
25
105°42'30"W
Qao
Qay
af
Qao
Qao3
Qao
Qao1
Qay
Qao2
105°45'0"W
Qao2
Qao2
Qao2
Qao3
Kc
4
Qao
Qao2
Qao2
Qao1
Qar
Qao2
Qao2 Qao2 Qao2
Qao2
Qao2 Qao2
Qao2
Qay
Qao2
Qay
afaf
Qay
Qay
Qao1
65
Qayr
Qao2
Qay
Qay
Qao2
Kg
3
8
Qao
? ?in active drainages, where the surface has
Recent alluvium (0–200 years old)—Well-stratified sand and gravel (primarily pebbles and cobbles)
?Qar ? fresh bar and swale topography up to 60 cm. Also commonly observed as small fan lobes at the mouths of recently incised arroyos, and as a
? ?
~
Qao2
Qay
Qao1
Qay
Qao1
Qse
Qar
Qay
Qay
Qao2
Qao1
Qse/Kg
Qay
Qao2
T-3271
5
Qay
Qao
Qse
Qay
Qay
Qao
Qse/Kmd
Qay
Qse/Kmd
Qao
Qao2
Qao
Qay
Qar
4
85 Py
Psr 6
3
Qse
Qse
10
3.0
Qao1
Kg
Kmd
3
Qay
^mKd15
5
Qao1
Qao1
Qse
Psr
Qse
Qao2 ALLUVIAL DEPOSITS
Qay
Qao2
20 Qse
Qao1
Qbm
6
10
11
Qay
Py
Qao2
Py
Py
Py 5
Qse
Psr
29
Py
Psr
11
6
33°37'30"N
Qse
Qao1
2.0
?
?
MW-11
Kclt
Kclt
Titb
Qse/Kc
Qao1
A' Geologic cross section
Late
11
A
Moraine
Qao and outwash deposits near Sierra Blanca (middle to upper Pleistocene)—Glacial moraine deposits noted by Moore et al. (1988) but
not accessible for description. Outwash deposits consist of very poorly sorted boulders, cobbles, and pebbles of crystalline rocks eroded from the
?
? Three Rivers stock (Moore et al., 1988).
? ?
veneer of laminated sand overlying Qay near active drainages. Occupies shallow valleys in the medial Three Rivers fan, where the sediment is
primarily clay, silt, and very fine- to fine-grained sand. Soil development is very weak to non-existent. 1–3 m thick.
Early
106°2'30"W
Psr
4
Kg
Qao2
Spring
OLIGOCENE
106°5'0"W
Qao2
Qse/Kmd 10
KmdQse
Kmd
Qtr
Qse/Kg
6
Qtr
10
af
Kg
Qao2
Kg
8
Qao1 Qao1 Qao2 16
Kg
Qay
Qao1
Kg Kg
Qse
Kg Kclt
Qse/Kc
Kclt11
14 Qse
Qse/Kc
9
8
1.0
EOCENE
Qbm
106°7'30"W
Qse/Kg
Foliation lineation
Qay
Qtg AND OUTWASH DEPOSITS
GLACIAL MORAINE
Millions of
years (Ma) scale change
0.1
SMC-31-3
Qao2
Quartz veins (Oligocene)—Milky quartz precipitated in veins.
qv
Late
Qbm
Qbm
Qse
Qbm
Qbm
Qbm
Qbm
Qbm
Qbm
Qbm
Qse
Qbm
Qbm
Qbm
Qse
Qbm
Qbm
Qbm
Qbm
Qbm
Kg 7
57
Qao3
Travertine (middle to upper Pleistocene?)—Thin to medium, tabular beds of gray to tan calcium carbonate near the western quadrangle border.
Qls
Microkarst topography common on the travertine surface. Probably deposited in a series of seeps or springs during paleoclimates
with higher
precipitation rates than today.
Qmo
Qmo
S4 inclined foliation
20
Qtr
100
S3 inclined foliation
66
Qao2
Qao2
Qay
Qay
Qbm
Qao2
Qay
Qse/Kg
Qbm
Qse
Qse
106°0'0"W
23
af
Qse
Qay
Qbm
Qbm
Qbm
Qao2
Qse
Qao1
Gypsum at the base of steep slopes west of Oscura (upper Pleistocene to Holocene)—Gypsum
in a tabular layer or possibly in an eolian sand
Qtr
sheet. Inferred to have been deposited by wind and then later experienced dissolution–precipitation events. 1 m thick?
Early
8
8
? ?
PRECIPITATE DEPOSITS
? ?
Late
^m
80
S2 vertical foliation
33°40'0"N
Qse
^m
Kd
Sheetflood–slopewash deposits and coppice dunes, undivided, overlying the middle subunit of olderQdsct
alluvium—See descriptions for units
Qsec (above) and Qao2 (below).
Km
Qao2
Qsec/Qao2
Qgy
Strike and dip of overturned bedding
Qay
Qay
Sheetflood–slopewash deposits and coppice dunes, undivided, overlying younger alluvium—See descriptions for units Qsec (above) and
Qay (below).
Qai
60
Qao2
Qao2
Qao2
Qsec/Qay
40
Strike and dip of inclined bedding
59
Qao2
(middle to upper Holocene)—Similar to unit Qse, but with 5% or greater surface coverage by coppice dunes. See descriptions of Qse and Qec
(above).
Shear zone
Strike and dip of vertical joint
Qay
33°40'0"N
10
20
Minor S-fold
Kc Qls
Tist
11
11
Qse
Minor M-fold
Early
Kd
^m
10
Cross bedding — Truncated foresets represent top
Qao2
6
Kml
Overturned syncline — Showing direction of plunge; dashed where approximately located; dotted where concealed
Middle
Kd
^m
Kd
Kml
Tist
5
Kml
KmlTist
Kd Tist
8
Qsec
PLIOCENE
^m
Overturned anticline — Showing direction of plunge; dashed where approximately located; dotted where concealed
Qay
Kg
Qbm
Kc
Kc
Kc
Qay
Tist
Kc
Tist
^m
Kd Tist
6
Qao2
Kg 6
Tita
QseQse
Qbm
Qse
Qse
Qse
Syncline — Showing direction of plunge; dashed where approximately located;
dotted where concealed
33°42'30"N
Qse
Qse
Qse
Qse
Qse Qse QlsQse
Qse
Qse
Qse
Qse Qse
Qse
Qse QseQse
Qse Qse Qse Qse
Qse
Qay Qse Qse Qse
Qse
Kc
Qao2
Qse/Kc
4
Ps
3
Kc
Kc
Qls
Kc
Qse/Kc
Kg
Anticline — Showing direction of plunge; dashed where approximately located;
dotted where concealed
10
44
3
Kc
Qse/Kc
Kc
Qao2
Kc
Kc
Qls
Kg
Qbm
2
35
5
Qao2
Qao2
Qbm
Qse Tist
Tist
5
6
Qse/Kg
KcQay Kc2010
16
Tist8
Qse
Tist
Qao2
Qls
9106
5
45
Qse/Kg
6Kg
10
Qls
Qse/Kc
Kg
Kg
Qse/Kg Kg
Kg 5
Kg
Qse
Kc
Qse/Kg
4
Kg
4 33
6 63
8
Kg 10 Kg
Tita
Tita
Kg6
Kg
Qse/Kg
Tita Kg
Kg
Qbm
Qbm
Kg
67
7
7
7
Qao2
Qse
4
Kg
Kg
Kg
78
Qao2
Qse
Qao2Qao2
3
33°42'30"N
Qao2
Qao2
Laramide reverse fault —Showing dip; barb on upthrown side; dashed where
approximately located; dotted where concealed
Qls
84
Qao2KcTist
Qay
Qao1
8
Kc TitaTist Qao2
0 Tist
Qao1
Tist
Kc 82
3
105°57'30"W
12
• • •
86 Qao2
Kg77
Kg
Kg
54
36
76
6
Qse
Kml
QseTist
9
Kml
5
QseTist
Qse Qao2
Kd
Tist
5 Qse
Kml
Kd
Tist
Kml
Tist
Qse
▲
Qao2
8
Qao2 Kg
Qec
Qao2
▲
55
Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the Crevasse Canyon
Qar Formation—See descriptions for units
af Qse (above) and Kc (below).
Qec
Qse,
Qe,
Qse/Tc
reworking a notable component
of eolian sediment, overlying the Gallup Sandstone—See
Qed,
Qse/Kg Sheetflood and slopewash deposits, probably
descriptions for units Qse (above) and Kg (below).
Qse/Kc,
Qec,
Qsec/Qay,
Qay,
Qse/Kg,
Qsec
Qse/Kmd Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the D-Cross Member of the
Qsec/Qao2
Qary, Mancos Shale—See descriptions
Qse/Kmd
for units Qse (above) and Kmd (below).
Qayr
Qse/Psf
Qbm
Qgy
Qct overlying the Four Mile Draw Member
Sheetflood
and
slopewash
deposits,
probably
reworking
a
notable
component
of eolian sediment,
&
Qse/Psf
of
the
San
Andres
Formation—See
descriptions
for
units
Qse
(above)
and
Kmd
(below).
Qay/
Qai Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, with coppice dunes on the surface
Late
Kmd
Qao2
Kg
Kg
2
Kmd
Qao2
KmdQao2
Qse/Kg
Kg
Kmd
Qse/Kg
Qse/Kg
Titb
Qao2
Qao2
Titb
Qse/Kg
Qse/Kg
tion—See descriptions for units Qse (above) and Tc (below),
Qse/Kc
Mid.
Qao2
Qao2
Miocene normal fault — Bar and ball on downthrown side; dashed where
approximately located; dotted where concealed
Early
Kg
• • •
15
5
Qao2
Qao2
Kg
Kg
Qao1
Qao2
Qao2
1
Qbm
Qbm
Qbm
Qbm
Qbm
Qao2
Thousands of
years (ka)
0
PLEISTOCENE
Qao2
Qao2
• • • • •
Qao2
Qao2
17
1
5
Qse
Qse/Tc
Contact — Dashed where approximately located; dotted where concealed
• • • •
14 9
Qao2
Time correlation chart for
map units in the northernTularosa Basin compilation map
Sheetflood and slopewash deposits, probably reworking a notable component of eolian sediment, overlying the Cub Mountain Forma-
HOLOCENE
9
Qao2Qao2
PLEISTOCENE
17
Qao2
Map Symbols
11
1262
Qao2
20
Qao2
Qao2
8 15
Qao2
Qao2
Qao2
Qao2 Qao2
Tist
Km
Tist
6C-339
Tita
Qdsct Kml
KtTist
Kmd Tist 8TistQao2
Timp
6
Tist
Kmd
Kmd
Tist Kml
Kmd Km
TistQao2
Qay
Kg
TistTistQdsct
Qay
Kmd
KtTist
White
Qdsct
Qao2
Kt Oaks
KmdTistKmdKt Qls
Kmd
Qao1
Qdsct
well
50
Qls TistKmdQay
Tist
Qao2Tist Tist
Kml
KmlQao2
Tist
Tist
Kml
Qay
KmdTimp
Qao2
Tist
Qao2
Qdsct
Qao2
7
7Tist
80
78
Tist 10Qao2
Qls
Timp
Qls
Qls Kmd
Qls
Qay
Kmd10
TistTimp
3Kt15Qay Qao1
Qao2
Qls
Qao2
7 Vega well
Tist 1 Kml
Gary
Qao2
Kml
Tist
Kt
Tist 0
Qao2
Kg
1 Kt
Qao1
Qao2
Kg Tist
Kml Qay
Kg
Kg
Qls
8
Kc
Qls
Kml
11
Kd
Qay
Qao2
14
Qao1
QTg Qao2
• • • • •
QTg
Qay
17 3
Qao2
Qao2
Qse
105°47'30"W
Qay
• • • • •
Qay Qay
Qay Kml
Tita
105°50'0"W
89
15
105°52'30"W
• • • • •
105°55'0"W
Twtat
Argentina Springs Tuff Member of the Three Rivers Formation (upper Eocene)—A lithic-rich, plagioclase-phyric, flow-foliated (rheomorphic)
ignimbrite. The ignimbrite intervals are black to gray to yellowish-tan, slightly welded to densely welded, and lithic-rich, with flattened pumice
(fiamme) with a maximum aspect ratio of ≥25:1. Lithic fragments consist of white chert to fine-grained sandstone and a variety of light to dark-colored volcanic rocks, including syenitic rocks. There appears to be a volcaniclastic sedimentary interval between two zones of strongly foliated
Comments to Map Users
A geologic map displays information on the distribution, nature, orientation, and age relationships of
rock and deposits and the occurrence of structural features. Geologic and fault contacts are irregular
surfaces that form boundaries between different types or ages of units. Data depicted on this geologic
quadrangle map may be based on any of the following: reconnaissance field geologic mapping, compilation of published and unpublished work, and photogeologic interpretation. Locations of contacts are not
surveyed, but are plotted by interpretation of the position of a given contact onto a topographic base
map; therefore, the accuracy of contact locations depends on the scale of mapping and the interpretation
of the geologist(s). Any enlargement of this map could cause misunderstanding in the detail of mapping
and may result in erroneous interpretations. Site-specific conditions should be verified by detailed
surface mapping or subsurface exploration. Topographic and cultural changes associated with recent
development may not be shown.
Cross sections are constructed based upon the interpretations of the author made from geologic
mapping, and available geophysical and subsurface (drillhole) data. Cross sections should be used as an
aid to understanding the general geologic framework of the map area, and should not be the sole source
of information for use in locating or designing wells, buildings, roads, or other man-made structures.
This map has not been reviewed by the New Mexico Bureau of Geology and Mineral Resources editorial staff and does not necessarily comply with NMBGMR GM series map standards. The contents of the
report and map should not be considered final and complete until reviewed and published by the New
Mexico Bureau of Geology and Mineral Resources. The views and conclusions contained in this
document are those of the authors and should not be interpreted as necessarily representing the official
policies, either expressed or implied, of the State of New Mexico, or the U.S. Government.