NMBGMR Open-file Geologic Map 151
Last Modified April 2010
NEW MEXICO BUREAU OF GEOLOGY AND MINERAL RESOURCES A DIVISION OF NEW MEXICO INSTITUTE OF MINING AND TECHNOLOGY
Qds
Qd
Qds
Qd
Qobp
Qe
Qlt1
Qds
Ql1
Qds
Qa
Qlt2
Qla
Qd
Qd
Qd
Ql
Qds
Qds
Qa
Qds
Qoae
Qbs
Qds
daf
Qlt1
Qds
Qd
Qe
Qlt3
Hmp2
hmp3
o
Psr
3 Qd
!
!
Qds
daf
Qocp
Qoae
Qlt2
Hmp2
Qds
daf
Qd
Qd
Qoae
Qd
Qe
Qd
Hmh2
!
60938
daf
Qlt1
daf
Qlt3
Qabp
Qbs
Qds
Qabp
Qafo
daf
Hmp2
Qa
Qoae
Psr
3700000
Modern meander belt deposits (Historic) — Very pale brown (10YR7/4) to reddish brown (2.5YR4/6), unconsolidated,
moderately to well-sorted, occasionally pebbly, coarse- to fine-grained sand in the modern channel and adjacent bar crests,
grading to silty sand and sandy clay with distance from the channel. In the early 1950s, two major meander cutoffs (along
with other minor channel adjustments) were carried out by the U.S. Bureau of Reclamation to create oxbow lakes out of the
large 1940s-era meanders in the BLNWR, thereby increasing open water and wetlands for waterfowl, aquatic plants, and
fish. As a result, the majority of the modern channel through its Bitter Lake reach has since been confined into old Qadp
channels, and meandering has been hampered. Modern meander amplitudes are only approximately 0.2-0.6 km in width.
This has greatly reduced overbank deposition, thus the majority of modern meander belt deposits are <1 m thick, but reach
about 1.5 m thick.
Qabh5
Qabh4
3699000
!
!
Qca
Qd
!
Qd
!
Qa
Qabp
!
Qlt1
hmp3
3
!
Qbs
!
daf
Psr
Qd
daf
Qlt3
Qa
daf
!
Qbt
Qabp
Hmp2
Qbs
Qds
Qabh2
A'
!
Qca
Qabh3
5
!
!
Qlt2
Qd
Qlt2
Qlt2
Qlt2
Qoae
Qaf
o
Qbt
daf
Qocp
Qd
Qlt2
Qlt1
daf
Qca
Qa
daf
Qabp
Qd
Qa/Psr
!
Qd
daf
Qlt2
Qlt2
!
Qlt2
Hmp2
daf
!
Qlt1
Qd
A
!
Qds
Qd
!
Qoae
!
Qlt2
Qlt3
Qlt2
!
daf
!
!
!
Qlt1
Qabp
Qbs
daf
Qd
Qbs
Qabp
daf
Qds
Qaf
Qds
Qd
Qd
Qds
!
Qa/Psr
!
Qabh2
Psr
Qd
!
Qabh3
Qah
!
Hmh2
daf
!
Qabh5
Qd
!
Hmh2
Hmh3
Qabh3
Hmh1
hmp3
!
Qah
!
!
!
Qabh4
daf
Hmh1
Hmp2
!
Qah Hmh3
Qoae
!
!
daf
hmp3
Hmh2
Hmh1
Hmh2
!
Hmh2
Hmh3
Qa/Psr
hmp4
o M
Qaf
Psr
Qds
Qa
!
Qabh5
!
!
!
Hmh2
!
Hmh3
Qabh1
!
Qlt2
Qabh1
Qabh1
Qa
Qds
Qds
!
Psr
Qabp
hmp3
Qd
Qa
Qd
!
hmp3
Qca
!
!
Psr
Qdp Qaf
Qd
Hmh1
!
daf
Hmh3
Qabp
Qds
Qds
Qds
Qds
Qds
Qds
!
Qds
!
hmp3
Qabh1
Qabh1
water
Hmh1
Qds
Qdp
Qds
Qd
Qa
Hmh1
Qa/Psr
Qdcp
!
Qabh1
daf
Hmh2
Hmh3
!
!
YO
!
!
Bu
Qoae
!
!
!
Qds
104°27'30"
551000
552000
Base map from U.S. Geological Survey1962, from photographs taken 1961.1927 North American datum,
UTM projection -- zone 13N
1000-meter Universal Transverse Mercator grid, zone 13, shown in red
0.5
1000
0
1
MELENA
554000
104°25'
555000
ACME
1000
0
2000
0.5
3000
5000
6000
0
7000 FEET
1 KILOMETER
A
A'
ROSWELL NORTH
SOUTH SPRING
557000
3693000
33°22'30"N
104°22'30"W
Hmp1
Location of geologic cross section.
?
Qdp
CONTOUR INTERVAL 10 FEET
Magnetic Declination
April 2006
8º 41' East
At Map Center
COMANCHE SPRING
NEW MEXICO
ROSWELL SOUTH
Hmh1
Geologic contact. Solid where exposed or known, dashed where
approximately known, queried where uncertain, dotted where
concealed.
Trace of syncline axial plane associated with evaporite collapse.
Dotted where concealed.
NATIONAL GEODETIC VERTICAL DATUM OF 1929
Bitter
Lake
Qd
Qd
Hmh2
Hmp2
Qd
EXPLANATION OF MAP SYMBOLS
1 MILE
4000
Qds
Qabp
556000
1:24,000
1
PANTHER HILL
553000
Qds
Qds
Qd
BOTTOMLESS LAKES
QUADRANGLE LOCATION
Mapping of this quadrangle was funded by a matching-funds grant from the STATEMAP program
of the National Cooperative Geologic Mapping Act, administered by the U. S. Geological Survey,
and by the New Mexico Bureau of Geology and Mineral Resources, (Dr. Peter A. Scholle,
Director and State Geologist , Dr. J. Michael Timmons, Geologic Mapping Program Manager).
Geologic map of the Bitter Lake quadrangle,
Chaves County, New Mexico.
Westernmost limit of gypsum soils, based upon the Chaves
County Soil Survey of 1980.
Horizontal bedding.
11
00175
W
Inclined bedding showing degrees of dip.
Oil well with last five digits of API number from NM Oil
Conservation Division database.
Qabp
May 2007
New Mexico Bureau of Geology and Mineral Resources
New Mexico Tech
801 Leroy Place
Socorro, New Mexico
87801-4796
by
David J. McCraw, Geoffrey Rawling, and Lewis A. Land
On this northwestern surface of Qoae, in addition to the depression and lacustrine deposits discussed below, two distinct
middle (?) Pleistocene Pecos River channels (Qocp) traverse from north to south-southwest. Alluvial channel and point bar
deposits associated with these Pecos channels (Qobp) are present in places. There is some suggestion of fluvial interaction
between the channels via Qa deposits, and depressions greatly influenced where these channels developed.
Younger Holocene meander belt deposits (Historic to upper Holocene) — Very pale brown (10YR7/4) to reddish brown
(2.5YR4/6), unconsolidated, moderately to well sorted, occasionally pebbly, coarse- to fine-grained sand, silty sand, and
sandy clay. Meander geometries are similar to hmp1, and while much of this is obscured by more recent meander belt
deposition and/or agriculture, amplitudes are estimated to average about 1 km in width with one amplitude of about 2 km
in width. Thickness 3-10 m.
Older Holocene meander belt deposits (upper Holocene to lower (?) Holocene) — White (2.5Y8/1) to light gray (2.5Y7/1)
in the northern part of the quad, very pale brown (10YR7/4) to reddish brown (2.5YR4/6) in the south, unconsolidated,
well sorted, fine-grained, gypsiferous (especially in the north) sand, silty sand, and sandy clay. Meander geometries are
significantly smaller with meander amplitudes averaging only 0.5 km in width. It appears that this meander belt was first
to develop, switching the river from flowing in a braided, coarser-grained Qabp floodplain into a small meandering stream,
which probably co-existed with active Qabp channels throughout much of the lower Holocene. The northern segment is
older than those deposits located at the mouth of the Rio Hondo, whose timing is constrained to the middle Holocene, as
discussed below. Nevertheless, the northern segment is also younger as it has been active throughout much of the Holocene,
acting as a yazoo stream flowing into the backswamp (Qbs) of and surrounding Bitter Lake. Thickness <1-3 m.
Qoae
Orchard Park terrace alluvial and eolian deposits, undivided (upper to middle Pleistocene) — Thickness 15-45 m.
Qocp
Orchard Park terrace ancestral Pecos River alluvial channel deposits (upper to middle Pleistocene) — Thickness
about 2-15 m.
Qobp
Orchard Park terrace ancestral Pecos River alluvial point and channel bar deposits (upper to middle Pleistocene) —
Thickness 1-2 m.
Qbt
Pecos River channel alluvium occupying coalescing depressions (middle Holocene to uppermost Pleistocene) — Light
reddish-brown (5YR6/4) to reddish brown (2.5YR4/6), unconsolidated, well sorted, fine-grained, gypsiferous sand, silty
sand, and clay thinly draped over the floor of depressions developed primarily in gypsum. Forms the lowest inset fluvial
deposit of the Pecos floodplain. The timing of the collapse or subsidence of the depressions is unknown, but their capture
of the Pecos River is constrained to lower Holocene – uppermost Pleistocene prior to or at the onset of Hmp1 development
and probably in the waning phases of active Qabp deposition. This is clear because the tributary Rio Hondo built two
lower to middle Holocene meander belts (Hmh1 and Hmh2) across both upper Pleistocene Rio Hondo braided alluvial
“deltaic” deposits (Qabh1 and Qabh5) and Qabp, into which Qabh1-5 drained. Hmh1 and Hmh2 are clearly distinguished
from any meandering Pecos River deposit by differing lithologies, sediment chararacteristics, and especially meander
geometries (Rio Hondo meanders are an order of magnitude smaller than those of the Pecos), and are clearly visible in
aerial photos completely crossing the Pecos floodplain to the eastern margin, where it joined the Pecos in its Qdp channel on
the Bottomless Lakes quadrangle southeast of the Bitter Lake quad (Rawling and McCraw, 2010). While Qdp flows could
have occurred concurrently in the depression channel(s) and parts of Hmp1, it was not until an avulsion occurred upstream
during the middle Holocene, which caused Hmp1 to build out across Hmh1 and Hmh2 in the vicinity of the historic meander
belts, thereby cutting these lower belts off and causing the Rio Hondo to develop Hmh3 to the south and west. Pecos River
alluvium is very thin in these channels (<1-2 m thick) and very little bank or bar formation occurred while Qdp was active.
The shallow, saline Chain Lakes now occupy Qdp on the Bitter Lake quad.
Blackdom Terrace alluvial deposits (lower Pleistocene to upper Pliocene) — Fiedler and Nye (1933) describe the
Blackdom terrace in northern Chaves County as isolated erosional terrace remnants 9-15.5 m above the Orchard Park
terrace. This perfectly describes the isolated high hills we map as Blackdom terrace on the Bitter Lake quadrangle. They
are comprised predominantly of chert and quartzite gravel in yellowish brown (10YR5/4) to reddish brown (5YR5/4),
unconsolidated, moderately sorted, coarse- to fine-grained, occasionally gypsiferous, sand and silty sand. Thickness 1530(?) m.
Qbt
upper
275
286
290
Psr
Pqg
Psa
Py
Pa
View of a small sinkhole and several depressions in the distance developed on the Orchard
Park terrace, just west of Bitter Creek in the BLNWR. More than 40 cm of gypsite is
exposed in the sinkhole wall.
Qd
Qds
Pecos River braided alluvial deposits (lower Holocene to upper Pleistocene) — Light reddish-brown (5YR6/4) to reddish
brown (2.5YR4/6), unconsolidated, poorly to moderately sorted, pebbly coarse- to fine-grained sand, silty sand, sandy clay,
and clay. Braided channels and bars typify the surface of Qabp. As discussed above, the thickness of Qabp is greatest on the
western margin of the floodplain, although buried, varies from 10 - 20 m. Large areas of Qabp are found on the floodplain
surface in the center and eastern margins of the valley, here the thickness varies from 3 m to <1 m.
Quaternary depression fill, primarily caused by subsidence (Historic to middle Pleistocene) — Unconsolidated, wellsorted, fine-grained (fine sands to clay) complexes of alluvial, colluvial, eolian, and occasional lacustrine deposits within
closed depressions created by either gradual subsidence or sudden collapse followed by gradual subsidence of underlying
gypsiferous carbonate terrane. These complexes are often significantly modified by stream erosion and deposition, playa
deposition, deflation, and mass wasting. Depression fills have been active since the middle Pleistocene and are usually 1-3
m thick but can reach thicknesses in excess of 30 m.
Quaternary sinkhole deposits, primarily caused by collapse (Historic to middle Pleistocene) — Eastern bluffs: boulders,
slump blocks, gravel, sand, silt, and clay filling dry sinkholes derived from local collapse of Psr. Thickness unknown,
probably 1-5 m for smaller sinks, quite likely several tens of meters for the larger ones (predominantly on the Commanche
Spring quad to the east). Western terraces: occasional cobbles, gravel, and slumped gypsite blocks in a fine-grained sandy
clay matrix. Most are submerged beneath the water table. Thickness <1-5 (?) m.
New Mexico Bureau of Geology & Mineral Resources
801 Leroy Place, Socorro, NM 87801
New Mexico Bureau of Geology and Mineral Resources
Ql2
Ql1
Qla
Quaternary lacustrine deposits, undivided (lower Holocene (?) to upper Pleistocene) — Unconsolidated, well-sorted,
fine-grained silty sands, silt, and clay deposited primarily by pluvial lakes fed by artesian springs. These deposits surround
the lower Holocene lacustrine units, and may have a significant alluvial component in their composition. Thickness 1-2 m.
Young Quaternary lacustrine deposits (predominantly Historic to lower (?) Holocene) — Greenish gray (Gley1, 5/5GY)
to greenish black (Gley1, 2.5/5GY), unconsolidated, well-sorted, fine-grained silty sands, silt, and clay deposited by lakes
fed by artesian springs. Occupies lowest, wettest landscape positions. Thickness 1-3 m.
Older Quaternary lacustrine deposits (Historic to upper Pleistocene) — Greenish gray (Gley1, 5/10Y) to gray (5YR5/1),
unconsolidated, well-sorted, fine-grained silty sands, silt, and clay deposited by lakes fed by artesian springs. Occupies area
surrounding Ql2, and is inundated less frequently. Thickness 1-3 m.
Quaternary lacustrine and alluvial deposits, undivided (Historic to upper Pleistocene) — Pinkish gray (5YR6/2) to
gray (5YR5/1), unconsolidated, well-sorted, fine-grained silty sands, silt, and clay. Usually lacustrine, but when water levels
are sufficiently high, fluvial action occurs depositing alluvium, especially along the margins of this unit. Thickness 1-3 m.
Pemian Artesia Group
Psr
Pqg
Seven Rivers Formation (Guadelupian - upper Permian) — White to pale gray gypsum, brick red, pale red, to orange
very fine sandstone, siltstone, and mudstone, and minor limestone. Exposed in bluffs along the east bank of the Pecos River.
Gypsum comprises up to 75% of the unit in the southern two thirds of the quadrangle. Gypsum content decreases gradually
northward, with concomitant increase in clastic interbeds. North of the latitude of the wildlife refuge headquarters, gypsum
comprises only about 25% of the unit. Gypsum beds are thin- to thick- to very thick-bedded, and massive to thin-bedded
to laminated internally. Red outcrop color is due to surface wash from the clastic interbeds. These clastic layers often have
veins of gypsum. Bedding is irregular and highly variable where gypsum content is high. As gypsum content decreases,
bedding becomes thinner and more planar, with less development of collapse features and slumping. Top of the bluff is often
capped by or covered with rubble of medium gray thin- to medium-bedded, crinkly laminated limestone. The top is not
exposed, but thickness is at least 75 m, based on the cross section.
Queen and Grayburg Formations, undivided (Guadelupian - upper Permian) — Cross section only. Completely
covered by terrace deposits or stripped.
Other Pemian Sedimentary Rocks
Psa
San Andres Formation (middle to upper Permian) — Light to dark gray and bluish gray limestone and dolomite. Limestones
and dolomites range from thin- to very thick-bedded, and are carbonate mudstones, wackestones, and grainstones. Freshly
broken surfaces are darker gray than weathered surfaces and often fetid. Silty and sandy beds are common. Presumably the
upper Bonney Canyon member of Kelley (1971). Thickness unknown.
Py
Yeso Formation, undivided (lower to middle Permian) — Cross section only.
Pa
Abo Formation, undivided (lower to middle Permian) — Cross section only.
REFERENCES
Eswaran, H., and Zi-Tong, G., 1991, Properties, genesis, classification, and distribution of soils with gypsum:
in: Occurrence, characteristics, and genesis of carbonate, gypsum, and silica accumulations in soils, Soil
Science Society of America, Special Publication no. 26, p. 89- 118.
Fiedler, A. G., and Nye, S. S., 1933, Geology and ground-water resources of the Roswell artesian basin, New
Mexico: U.S. Geological Survey Water-supply Paper 639, 372 p.
Kelley, V. C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and
Mineral Resources Memoir 24, 78 p.
Depression, sinkhole, and lacustrine deposits
Kelley, V. C., 1980, Gatuña Formation (Late Cenozoic), Pecos Valley, New Mexico and Trans-Pecos Texas: New
Mexico Geological Society, Guidebook 31, p. 213-217.
Lyford, F. P., 1973, Valley fill in the Roswell-Artesia area, New Mexico: U.S. Geological Survey Open-file Report
73-163, 26 p.
Powers, D. W., and Holt, R. M., 1993, The upper Cenozoic Gatuña Formation of southeastern New Mexico: New
Mexico Geological Society, Guidebook 44, p. 271-282.
Rawling, G. and McCraw, D. J., 2010, Geologic map of the Bottomless Lakes quadrangle, Chaves County, New
Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file Geologic Map 126, 1:24,000.
Watson, A., 1983, Gypsum crusts: in: Pye, K., and Goudie, A. S., eds., Chemical sediments and geomorphology:
precipitates and residua in the near-surface environment, Academic Press, London, p. 133-161.
GEOLOGIC CROSS SECTION
COMMENTS TO MAP USERS
Pecos River
terraces (Qlt1-3)
over Seven
Rivers Fm
Open-file Geologic Map 151
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.
(575) 835-5490
This and other STATEMAP quadrangles are available
for free download in both PDF and ArcGIS formats at:
http://geoinfo.nmt.edu
Pecos River terraces (Qlt1-3, Qoae, Qbt)
West
4,000 ft
ASL
Late afternoon view across Bitter Lake to the eastern Permian bluffs and uplands of the Seven Rivers
formation at the eastern margin of the Pecos floodplain. Numerous snow geese can be seen on the lake. At
the base of the bluffs on the left, the Lakewood and Orchard Park terraces are evident.
The map has not been reviewed according to New Mexico Bureau of Geology and Mineral Resources
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.
A'
Y-O
Buckle Pecos
Berrendo
Creek
3,000’
East
River
Pqg
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 not be the sole source
of information for use in locating or designing wells, buildings, roads, or other man-made structures.
Pecos River floodplain
A
2
550000
Hmp2
Hmh3
Qds
Qd
daf
!
549000
Qds
Qds
!
Qa
Qa
hmp4
!
Qahf3
A southwesterly view of both the modern, sediment-laden, reddish-brown, muddy Pecos
River and its meander belt in the foreground and a sweeping 1939-40-vintage meander,
now a quiet-water, oxbow lake in the upper distance. The lower of the two major 1950s
cutoffs occurred just out of the picture to the left.
Qd
!
le
Qoae
ck
Qahf3
!
daf
3694000
Qaf
Qdp
!
!
daf
Qd
Qds
!
!
!
Hmh3
Qlt3
hmp3
Hmp2
!
daf
548000
Qds
PALEOZOIC SEDIMENTARY ROCKS
The remaining two areas of Orchard Park terrace are separated by the Hondo valley. The southern area lies west of the
gypsiferous soils and saline ground-waters, and again, supports extensive agriculture. It is comprised of very pale brown
(10YR7/4) to reddish brown (5YR4/4), unconsolidated, moderately sorted, coarse- to fine- grained sand, silty sand, silt, and
sandy clay. The northern area, however, is predominantly gypsiferous with saline ground-waters. It is comprised of white
(2.5Y8/1) to light gray (2.5Y7/1) to very pale brown (10YR7/4), unconsolidated, well sorted, fine-grained, gypsiferous sand,
silty sand, and sandy clay. In general, the gypsum content of the soils decreases from the western bluffs above the Pecos
valley westward. At and near the bluffs, Qoae is so choked with gypsum it forms gypsite, an indurated hyper-concentration
of gypsum in the soil (Watson, 1983). This material develops from a combination of in-situ weathering of gypsum bedrock,
as well as eolian and alluvial depositional input of gypsum into the solum (Eswaran and Zi-Tong, 1991).
Qd
Qa/Psr
!
Qa
3694000
Qds
Qd
Qabh1
!
Hmh1
Qd
Hmh1
!
Qlt1
Qds
Qds
Qa/Psr
!
!
!
Qa
Qoae
Qa
Qds
Qds
Qd
Qds
Hmh1
Hmp1
Qaf
Psr
Hmp1
!
daf
daf
3693000
268
On the Bitter Lake quadrangle, the Orchard Park terrace comprises the majority of the surface area, in three distinct
locations: the northeast corner of the quad, the western two-thirds of the quad north of the Hondo Valley, and the agricultural
lands south of the Hondo valley, west of the Pecos floodplain. The northeastern deposit is distinctly different from the
other Orchard Park deposits as its largely non-gypsiferous, made up of light reddish-brown (5YR6/4) to reddish brown
(2.5YR4/6), unconsolidated, moderately sorted, pebbly, medium- to fine-grained sand, and silty sand. This deposit could
actually be an outcrop of the Gatuña Formation (Kelley, 1980; Powers and Holt, 1993) as the lithologic characteristics are
essentially identical, but given its proximity to the Pecos floodplain, is mapped as Qoae.
3695000
!
Qdp
Hmh1
!
!
Qah
!
Qabh1
Qoae
Older Lakewood terrace alluvial deposits (upper to middle Pleistocene) —Thickness about 2-9 m.
Qca
Hmp1
hmp4
Hmh1
daf
!
daf
hmp3
Hmh1
!
Hmh3
3695000
Qoae
Qlt1
Qdp
daf
Hmh1
Hmh2
!
Qlt1
Qoae
Young Lakewood terrace alluvial deposits (upper Pleistocene) —Thickness 1.5-5 m.
Orchard Park terrace alluvial deposits (upper to middle Pleistocene) — According to Fiedler and Nye (1933), the
Orchard Park terrace rises 1.5-3 m above the Lakewood terrace and 6-10.5 m above the Pecos floodplain. On the Bitter Lake
quadrangle, it consists of an alluvial-eolian complex (Qoae), with many subsidence-related depressions (Qd) and collapserelated sinkholes (Qds) pitting its surface. Furthermore, many of these depressions are artesian-spring fed, and supported
shallow lakes (Ql, Ql2 ,and Ql1) prior to 20th Century pumping of the artesian aquifer. Given their shallow nature, water
often flowed from basin to basin, giving rise to an unusual “hybrid” lacustrine-alluvium map unit (Qla).
e
e
Qah
daf
Qah
Qah
!
Hmh3
!
Hmh2
Hmh2
Qlt3
5
!
Hmh1
Hmh2
!
Hmh3 Hmh2
Hmh3
Qlt1
Qlt2
7
daf
!
Qah
Qabh5
Qah
!
Hmh1
Youngest Lakewood terrace alluvial deposits (upper Pleistocene) — Thickness <1-1 m.
!
Hmh2
Hmh3
Qlt2
Hmh1
3696000
Qd
Qlt3
Hmp1
hmp3
!
Hmh1
Qd
Qd
!
Qlt1
Hmh2
Qd
Qds
!
Hmh2
hmp4
!
Qabh5
Qlt3
Qah
Qabh5
!
Qah
Hmh1
daf
Qd
1939-1940 meander belt deposits (Historic) — Very pale brown (10YR7/4) to reddish brown (2.5YR4/6), unconsolidated,
moderately to well sorted, coarse- to fine-grained gypsiferous sand in the Historic channel and adjacent bar crests, grading
to silty sand and sandy clay with distance from these older channels. Throughout the upper Holocene, extensive point bar
development has taken place, resulting in a series of meanders, with meander amplitudes >1 km in width common, the
largest reaching about 1.8 km in width. In terms of estimating thicknesses of this meander belt, the Holocene meander
belts, and the braided Pleistocene deposits, we consider a valley-fill thickness map based upon interpretations of data from
numerous wells throughout the Roswell artesian basin by Lyford (1973). This map depicts the valley fill thickness dropping
from approximately 30 m at the base of the western Orchard Park terrace bluffs to < 1 m just west of the modern channel.
Based upon this fact that the meander belts are built on a wedge of Pleistocene braided alluvial valley fill, present at the
surface aside hmp2 and buried with a ~30-m base alongside the western bluffs, the thickness of hmp1 ranges from <1 m to
3-10 m where it overlies Holocene meander belts, and up to15 m where it buries Qabp.
6198
Psa
Hmh2
!
daf
Hmh3
!
Hmh3
Hmh2
hmp3
!
Qah
!
Qah
Qabh4
daf
Qds
!
Hmh2
!
Qah
Qah
547000
hmp3
!
Hmh3
Qah
33°22'30"N
104°30'00"W
3697000
!
Qabh2
daf
Hmh2
264
!
!
!
!
!
!
!
Qabh2
Hmh2
Hmh2
Hmh2
Qah
!
Qabh2
W
62292
Qds
Qds
The modern Pecos River, here occupying an older braided Qadp channel, is incised into
Seven Rivers formation gypsum in the northeastern part of the quadrangle. Dormant salt
cedar (Tamarix pentandra), growing along the shore on the right, are approximately 1.5 m
in height. Note that the alluvium on top of the gypsum is <1 m in thickness.
33°25'
Qds
!
Qoae
daf
Qlt2
Qabp
!
Qds
Qlt3
Hmh3
Hmh3
Qds
!
Qlt2
Qabh2
Hmh3
hmp3
Qlt3
Qca
Qah
3697000
Lakewood terrace alluvial deposits (upper to middle Pleistocene) — Alluvial terraces of the Pecos River and its
tributaries were first described in the classic study of Fiedler and Nye (1933). They recognized 3 terraces: (from lowest to
highest) the Lakewood, the Orchard Park, and the Blackdom. The Lakewood terrace, with an elevation of 6 to 9 m above
the floodplain, flanked the inset Pecos floodplain and extended up many of its western tributaries. We now recognize three
distinct low-lying (upper to uppermost middle(?) Pleistocene) “Lakewood terraces,” the highest and oldest of which would
be Fiedler and Nye’s original. Surface tread elevations above the floodplain for these three are: <1-1 m, 1.2-6 m, and 6-9 m,
respectively. These terraces are differentiated by their location either in the Pecos valley or in the tributary valleys of the Rio
Hondo and Borrendo Creek, and its tributaries. The Pecos valley west side terraces are comprised of light gray (2.5Y7/1) to
very pale brown (10YR7/4) to reddish brown (2.5YR4/6), unconsolidated, well-sorted, medium- to fine-grained gypsiferous
sand, silt, and sandy clay, while the east side terraces are made up of light reddish-brown (5YR6/4) to reddish brown
(2.5YR4/6), unconsolidated, moderately sorted, pebbly, fine-grained, gypsiferous sand, silty sand, and clay. The tributary
Lakewood terrace alluvial deposits are comprised of occasional gravels and pebbles, brown (10YR5/3) to dark yellowish
brown (10YR3/4), unconsolidated, moderately sorted, coarse- to fine- grained sand, silty sand, silt and sandy clay. These
sediments are mostly non-gypsiferous.
Qd
daf
e
Hmh3
Qlt2
Qa
3.6
261
Ql
!
Qca
Qlt2
Qlt3
Qah
!
Qah
Hmh3
Qoae
Qd
1.8 Ma
Oldest braided valley-mouth alluvial-fan deposits (upper to middle (?) Pleistocene) — Lowest-lying, yet most extensive
braided alluvial-fan deposit. Greatly modified by agriculture on it eastern margin adjacent to and within the Pecos floodplain.
Only an occasional channel remnant remains. Overriden by Qabh5, Hmh3, and Hmp2. Thickness about 2-30 m.
3698000
Qds
!
Qlt3
Qbs
Qa
daf
Qocp Qobp
Qoae
780
Alluvial terrace deposits
!
Qabp
daf
Qca
Qlt2
Qbs
Qlt3
Qlt1
Qlt1
Older braided valley-mouth alluvial-fan deposits (upper Pleistocene) — Lower, northernmost Qabh deposit exhibiting
large areas choked with gypsite crust, few channel scars remaining, and wide areas of extensive deflation. Often undergoes
modern flooding. Thickness about 2-10 m.
Qd
!
Hmp2
daf
Qabp
!
Qlt2
daf
33°25'
Psa
Hmp2
Qca
Qlt2
Qca
Qlt3
Qabh1
!
!
Qd
daf
daf
daf
W 62232
daf
daf
Qlt3
Qabh2
Qafo
Young braided valley-mouth alluvial-fan deposits (upper Pleistocene) — Highest Qabh deposit suggesting formation
during periods of massive outwash deposition. Large areas choked with gypsite crust, minor channel remnants remain.
Thickness about 3-20 m.
!
Qlt1
Qlt2
!
Qlt2
daf
!
Qoae
Qlt2
Ql1
Younger braided valley-mouth alluvial-fan deposits (upper Pleistocene) — Surface slightly higher, channels less
defined and more braided (multiple, smaller channels) with more extensive gypsite at the surface than Qabh5. The 2005
orthoimagery shows approximately the eastern quarter of this deposit with a distinctly redder surface, in a semi-arcuate
shape, suggesting a possible short-lived Hmp2 occupation of this lowland. Thickness <1 to about 15 m.
8
!
Qd
Qlt3
Qabh1
Psr
!
Qca
Qd
daf
3698000
Qabh3
Ql
hmp3
hmp4
!
daf
!
Qlt1
!
Qoae
daf
!
Qlt1
Qbs
Qlt2
Qabp
Qla
Youngest braided valley-mouth alluvial-fan deposits (uppermost Pleistocene) — Clearly defined channels are seen
on the second-lowest Qabh surface, including a large (i.e., very high meander wavelengths and amplitudes compared to
the Holocene Rio Hondo) channel, overridden in places by Hmh1-2. Bar and swale deposits exhibit minor gypsite crust
development. Qabh5 spreads out laterally both north and south at the margin of Pecos alluvial deposits (both braided and
meandering) due to the fact that it accommodates Holocene to modern flows from older Qabh valley-mouth fan channels.
Thickness <1 to about 15 m.
o
Qa
Qaf
Psr
Qa/Psr
!
Hmp2
Qlt3
daf
3696000
hmp3
Qocp
Qoae
daf
Qah
!
Qd
!
Qlt3
Qlt2
Qd
Qd
Qlt3
Qabh4
!
Qbs
Qlt1
Qlt3
!
Qlt3
!
Qlt3
o
Qoae
Older Holocene meander belt deposits (middle Holocene to lower (?) Holocene) — In the Hondo floodplain, Hmh1 flowed
primarily along the southern margin (mapped where not totally obscured by agriculture), probably in upper Pleistocene
channels. At the mouth of the floodplain, its course was clearly influenced by the youngest upper Pleistocene channels
within Qabh5. Thickness 1-3 m.
Rio Hondo braided alluvial deposits (lower Holocene to upper Pleistocene) — Cobbles and gravels of chert, quartzite,
gray and green porphyritic igneous rocks, and limestone in brown (10YR5/3) to dark yellowish brown (10YR3/4),
unconsolidated, poorly to moderately sorted, coarse- to fine- grained sand, silty sand, silt (largely calcareous), sandy clay,
and clay. From the mouth of the Hondo floodplain westward up the valley, these braided deposits are either all buried or
undiscernable due to agriculture. They undoubtedly fill the entire base of the inset valley and are probably 15-30 m thick.
As these upper Pleistocene braided stream channels carrying glacial outwash from the Sacramento Mountains discharged
out into the Pecos floodplain, they built a series of “deltaic” valley-mouth fans, each comprised of braided distributaries and
overbank deposits. These “deltas” can be differentiated based upon height above the Pecos floodplain, degree of channel
preservation, degree of deflation, and relative gypsite crust development into five distinct braided alluvial deposits. With the
exception Qabh1, the southernmost unit, units Qabh2-5 progressively shift from a northern position adjacent to the Hondo
floodplain Qbs deposits, southward approximately to the location of the Holocene Rio Hondo meander belts.
!
Qd
hmp4
Qlt1
W
Qd
Hmh1
Quaternary valley-fill alluvium over Seven Rivers formation, undivided — Light reddish-brown (5YR6/4) to reddish
brown (2.5YR4/6), unconsolidated, moderately sorted, pebbly, fine-grained, gypsiferous sand, silty sand, and clay, thinly
draped over gypsum, siltstone, and sandstone of Psr. Alluvium is <1 m (often <60 cm) in thickness.
Young meander belt deposits (middle Holocene) — As described above, the two oldest Hondo meander belts (Hmh1 and
Hmh2) built up on top of both upper Pleistocene Rio Hondo braided alluvium (Qabh) and upper Pleistocene Pecos braided
alluvium. In the Pecos floodplain, Hmh2 built on top of Hmh1, but in the Hondo floodplain, it built a new meander belt north
of Hmh1 until it reached the vicinity of the present-day Hagerman Canal diversion, where it crossed over Hmh1 and flowed
to the south, over Qabh1. Thickness 1-3 m.
8
Qlt1
Qaf
!
daf
Qoae
Qlt3
Qds
Qlt1
Qafo
!
Qlt3
daf
Qlt3
Qd
Qlt1
Qabp
Qbs
Qd
Psr
!
Qoae
Qaf
!
Qds
hmp3
hmp4
!
Qd
Qlt2
Eolian sand, undivided (Holocene – uppermost Pleistocene) — Very pale brown (10YR8/2) to light brown (7.5YR6/4),
unconsolidated, moderately to well-sorted sand, silty sand, and sandy clay. Forms extensive thin sheets and low dunes along
the top of the Orchard Park terrace (Qoae). Thickness commonly <1 m to about 3 m.
Modern (pre-channelization) meander belt deposits (Historic to upper Holocene) — Responding to an avulsion of the
Pecos River in the middle Holocene which shifted flow back to the west-central part of the floodplain into the Hmp1 deposit,
Hmh3 after leaving the Hondo floodplain was forced to turn south and build a course over the top of the oldest and lowest
Rio Hondo braided alluvial “deltaic” deposit (Qabh1). Upstream of this southerly diversion, Hmh3 basically built up on top
of Hmh2. It was abandoned in the early 20th Century with the construction of the Hagerman Canal and the channelized Rio
Hondo. Thickness 1-3 m.
6093
Qoae
Qds
Qd
Hmh3
2
Qlt2
17
15
Qabp
!
Qocp
Qds
!
Qa
3701000
Qd
o
Qbs
Qd
Qlt1
Qa
Qabp
Qlt3
Qds
Qlt1
3700000
daf
Qlt2
Qoae
Qla
Qlt1
Qa
hmp3
!
Qlt2
Psr
Qa
!
Qlt3
3701000
Hmp2
Qca
Qa
64982
Colluvium and/or valley-slope alluvium, undifferentiated (Holocene – uppermost Pleistocene) — Light reddish-brown
(5YR6/4) to reddish brown (2.5YR4/6) (eastern Psr bluffs), light gray (2.5Y7/1) to pale brown (10YR6/3) (Orchard Park
terrace and oldest Lakewood terrace margins), unconsolidated to poorly consolidated, poorly to moderately sorted sand and
silty sand, with rubble blocks of gypsum, sandstone, siltstone, and mudstone, and minor limestone (eastern Psr bluffs), and
blocks of indurated gypsite along the terrace bluffs. Deposits range from less than 1 m to about 3 m in thickness.
Pecos River meander belt alluvial deposits (Historic to lower (?) Holocene) — During the Holocene, the Pecos River
built four distinguishable meander belts on top of an upper Pleistocene Pecos River braided alluvial valley-fill deposit
(Qabp), which is the basal unit of the floodplain. Consisting of channel, channel bar, and point bar deposits, undivided, these
meander belt deposits are differentiated based upon aerial photographic work into two older Holocene units and two Historic
units: 1) the modern meander belt was mapped from both 2005 digital 1-m resolution, color orthophotography and 1981vintage color aerial photography produced for the U.S.D.I. – Bureau of Land Management, and 2) a 1939-1940 meander
belt was mapped using vintage U.S.D.A. – Soil Conservation Service black and white aerial photography. The 1939-40
meander belt, in places, also incorporates areas where meander migration clearly continued up at least until around 1962,
the issue date of the Bitter Lake topographic quadrangle (before photo-revision). The historic units are differentiated from
the Holocene units by using a lower case “h” on the unit labels.
!
Ql2
Qlt3
Qbs
!
Qlt2
daf
Qa
Qds
Qds
W
Qlt1
Qca
Qa
Qla
Qa/Psr
3702000
daf
Qabp
Qbs
Qocp
!
Qe
Qd
Qds
Qds
Qds
Qlt1
33°27'30"
Qoae
Qd
Psr
!
Qds
Rio Hondo meander belt alluvial deposits (Historic to lower (?) Holocene) — Cobbles and gravels of chert, quartzite,
gray and green porphyritic igneous rocks, and limestone in brown (10YR5/3) to dark yellowish brown (10YR3/4),
unconsolidated, moderately sorted, coarse- to fine- grained sand, silty sand, silt (largely calcareous), and sandy clay. While
meander geometries are essentially identical between all three Hondo meander belts, Hmh1 certainly exhibited the widest
lateral migration.
Hmp2
Qbs
Qbs
Qds
Qds
Qd
Qds
Qlt1
Qd
Qocp
Qe
Qoae
Qds
Qds
Qds
Qds
Qlt3
Qds
Quaternary valley-fill alluvium within the Rio Hondo, undivided (Historic to upper Pleistocene) — Cobbles and gravels
of chert, quartzite, gray and green porphyritic igneous rocks, and limestone in brown (10YR5/3) to dark yellowish brown
(10YR3/4), unconsolidated, poorly to moderately sorted, coarse- to fine- grained sand, silty sand, silt (largely calcareous),
sandy clay, and clay. While clasts and coarse-grained sediment are common, these deposits are typically found between
meander belts and older Pleistocene channel deposits, and are thus finer-grained. According to Lyford (1973), the valley fill
beneath the Hondo valley in the Bitter Lake quadrangle increases from about 30 m in thickness at the mouth to over 45 m
quickly upvalley. Thicknesses of Qah are estimated to be 10-25 m.
Qah Qabh5
Pqg
4,000 ft
ASL
2
Qla
Qd
128
Qbs
6229
Ql1
Qds
Qoae
Alluvial-fan deposits (Historic to upper Pleistocene) — Predominantly quartzite, chert, and carbonate cobbles to gravel,
often in stringers, in a light reddish-brown (5YR6/4) to reddish brown (2.5YR4/6), unconsolidated, poorly sorted, and
coarse- to fine-grained sand to silty sand. These fans are built along the base of the Seven Rivers formation (Psr) eastern
bluffs and interfinger with and/or spread out onto Pecos floodplain deposits. Subdividing the unit into an upper (Qaf) and
lower, older (Qafo) deposit was only clearly mappable for one fan. Thickness <1 m at their distal margins to 8 (?) m.
Pecos River alluvial valley floor
Qabp
Qds
Qoae
Qa
daf
Qds
Qd
Qah
Valley-slope alluvium with eolian sand (Holocene to upper Pleistocene) — White (2.5Y8/1) to light gray (2.5Y7/1),
unconsolidated to partly consolidated, well-sorted, fine-grained gypsiferous sand, silty sand, and clay along the northeast
slope of Lost River. Forms a relatively thin mantle of alluvial slope deposits shed off of the Orchard Park terrace uplands
combined with a large eolian component blown out of the Lost River floodplain, which is about 0.5 km wide here. Thicknesses
varies from <1 m immediately adjacent to Lost River to 2.5 m downslope of the alluvial terrace (Qoae).
daf
Qd
Qds
Qd
Rio Hondo alluvial valley floor
Qabp
Qlt2
Qds
Qd
Ql2
Qa
Qds
Qd
Qoae
hmp4
Qds
Qds
Qa
Qbt
33°27'30"
Qoae
Qe
Ql1
daf
Qe
Qlt3
!
Qla
Qocp
Qoae
Qds
Ql
3703000
Qlt3
Ql2
Ql2
Qd
Qa
Hmp1
Qbs
!
Ql2 Ql1
Ql1
Qlt1
Qds
Qd
Qlt2
Qlt2
Qa
Qd
Qds
Qlt3
Qlt2
Qds
Qds
o
Psr
Quaternary tributary alluvium and valley-fill alluvium, undifferentiated — Brown (7.5YR4/2) (Rio Hondo tributaries),
pinkish gray (7.5YR6/2) to light reddish-brown (5YR 6/4) to reddish brown (2.5YR4/6) (Pecos floodplain), unconsolidated,
moderately sorted, pebbly sand, silt, and clay, gypsiferous in Orchard Park terrace and Pecos floodplain areas. Varies
considerably in thickness from <1 m to 10-12 m.
6223
Ql2
hmp3
daf
Qds
3
Qa
!
Ql1
Ql2
3703000
Qoae
Qa
Qla
Qlt2
Qds
Qds
Qd
Qd
Qlt3
!
Qla
Qoae
Qa
Qd
Qca
Qlt3
Qds
Qoae
Qlt3
Qlt3
Qds
Ql1
Ql2
Qbt
Qds
Hmp2
Hmp1
!
Ql2
Qabp
Qlt3
Qlt1
Qds
Qbt
Qlt3
Qa
Qocp
Ql1
3704000
Qafo
Hmp1
Qbs
Qds
Qd
Qds
Qabp
Qa
Qlt3
Qds
Qds
Qoae
Ql2
Ql
Ql1
Qla
Qe
Qlt2
!
Qoae
Qa
Qd
Qaf
Qabp
!
Qoae
Ql
Qabp
Hmp2
Qa
Qlt2
Qds
Qd
Qa
daf
!
Ql2
Qoae
Qds
Qobp
Qlt3
Qbs
Qds
Qds
Hmp2
!
Ql
Qbt
Qabp
Qa
Qds
Qds
Psr
Hmp2
daf
Qds
!
Qe
Qae
Qa
!
Qe
Ql2
Qlt2
Qobp
Ql1
Qoae
hmp4
Qbs
daf
Qds
Qds
Qd
3705000
Qabp
!
3704000
Qds
Hmp1
Qds
Qds
Ql1
Qds
Qd
Qds
Qd
Qlt1
!
Qbt
Qds
Qds
Qlt3
Qds
daf
Qlt2
Qds
Qa
Qd
!
Ql1
daf
Qds
Qds
Qd
Qbt
Qabp
Qds
Qa
Qlt2
Qa/Psr
Qlt1
Qd
Qds
Qds
Qe
Ql2
Qds
!
Qoae
Qds
Qds
Qoae
daf
Qds
Qds
Qds
Qd
Qe
Qla
daf
Qa
Qd
Qdp
middle
Qds
Qoae
Qla
Qd
Qd Qds
Qd
Qoae
Qds
Qds
Qe
Qe
Qds
Qds
Qlt3
Qca
Qa
Psr
lower
Qd
Ql2
Qds
Hmp2
Hmp1
Qlt3
Qocp
Qla
Hmp1
Qds
Qds
Qds
Ql1
3705000
Qlt2
Qlt3
Qds
Hmp2
!
Qoae
Qd
Qd
Qd
daf
Qds
Qds
Qd
Ql2
Qoae
Qbt
Qd
Qlt1
Qae
Ql2
upper
Qae
Qe
Ql1
Qd
Qds
Qds
Qa
Bedrock
Artesia Group
Seven
QueenGrayburg Fms Rivers Fm
daf
11
Qe
Qaf
Hmh3
Hmh2
Hmh1
Depressions, sinkholes, and
lacustrine deposits
San Andres
Fm
Qds
Holocene
hmp4
hmp3
Hmp2
Hmp1
Alluvial terrace
deposits
Yeso
Fm
Qe
daf
Qds
daf
Qds
Qa
Qds
Historic
Rio Hondo
alluvial valley floor
Abo
Fm
Qa
daf
Artificial fill (Historic) — Disturbed areas, dumped fill, and areas affected by other human disturbances. Mapped where
deposits or extractions are areally extensive. Includes impoundment levees in the inundated backswamp (Qbs) areas within
the Bitter Lake National Wildlife Refuge (BLNWR), the channelized Rio Hondo, North Spring River, and the Hagerman
Canal, the BNSF railroad right-of-way, raised roadways along U.S. Highways 380 and 70, the old Desalinization Plant Brine
Field, the Roswell Country Club lake, and borrow or gravel pits.
Pecos River
alluvial valley floor
0 ka
Pleistocene
Qoae
Qds
3706000
Qlt1
!
Ql1
Qoae
hmp3
!
Ql1
Qlt2
Qlt3
Qds
Qlt2
daf
Qd
Qe
Qlt2
daf
Qds
Alluvium, colluvium, eolian, and anthropogenic deposits
Hmp2
Qabp
Qbs
Alluvium, colluvium,
and eolian deposits
Pliocene
Qds
Qd
Ql1
Qoae
Qlt2
Qd
Qoae
daf
Qlt3
Qds
Qds
Y-O
Qe
Qd
Qabp
Floodplain alluvial backswamp deposits (Historic to upper Pleistocene) — Pecos floodplain: light gray (2.5Y7/1) to
very dark gray (7.5YR3/1), unconsolidated, well-sorted, gypsiferous silty sand, sandy clay, and clay in low-lying, poorly
drained areas surrounding Bitter Lake and the impoundments along the western margins. Rio Hondo floodplain: light
brownish gray (10YR6/2) to dark yellowish brown (10YR3/4), unconsolidated, well-sorted, gypsiferous silty sand, sandy
clay, and clay in low-lying, poorly drained areas below the northern bluffs of the oldest Lakewood terrace (Qlt1). Both
areas commonly only receive fine-grained, slack-water flood deposition, although several springs discharge into the Pecos
Qbs. The Rio Hondo Qbs area occupies the lowest inset area in its floodplain, and is probably the result of scour from a
Pleistocene Rio Hondo channel. Thicknesses range from 3-15 (?) m in the Pecos floodplain and are unknown in the Rio
Hondo floodplain, but probably 3 m or less.
Permian
daf
Qd
Qd
Qd
Qd
Qocp
Quaternary/Neogene
Qlt1
hmp4
daf
Qds
Qds
Qlt3
Quaternary
Qoae
Ql2
Qlt3
Qlt1
Qlt2
Qlt1
Hmp2
Hmp1
Qa
Neogene
Qd
Qa
CO RRELATI O N O F M AP UNI TS
Paleozoic
Qocp
Ql2
3706000
Qoae
Qds
Qds
o
M
daf
Qd
Qd
!
Qoae
Qd
Qlt2
Qoae
Qd
DESCRIPTION OF MAP UNITS
104°22'30"W
33°30'00"N
Qoae
557000
!
Ql1
Qe
Qocp
Qoae
Qa
Qd
556000
!
Ql1
Ql
Qd
Qd
Qd
555000
!
Qe
daf
Qd
Ql1
104°25'
553000
!
Ql1
Qoae
552000
kle
551000
!
104°27'30"
Bu
c
550000
o
33°30'00"N
549000
!
548000
547000
!
104°30'00"W
Psr
Pqg
Psa
3,000’
Psa
Psa
2,000’
2,000’
Py
Py
1,000’
0’ Mean Sea Level
Pa
Pa
Py
1,000’
0’ Mean Sea Level