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f f f f f f f f f f f f f f f f f f f f f f f f f î o î î " F F F 7 Psd Qd Qds daf Qps4 Psg Qps4 Tps1 Qps4 Qd Qps3 Qps5 Psg Qps4 daf Qps3 Qps5 Qps4 Qps3 Qpsc2 QTps2 Qps3 QTps2 Qps4 Tps1 Qd Qps4 Qd Qa Qps3 daf daf daf Qpsc2 Qps4 Qps3 QTps2 Qpsc1 QTps2 Qbs Qd Qd Qps3 daf Qps4 Qps4 daf Qps4 Qpsc2 daf QTps2 Qps4 Qps4 Qps3 Qps4 Qd Qps5 Qps3 Qps4 Qps4 Qps3 Qps3 QTps2 Tps1 Qps4 QTps2 QTps2 Qps5 Qps3 Qps3 QTps2 daf Qps3 daf Qps5 Qps4 Qps4 Qps4 Qpsc2 Qps3 Qps4 QTps2 Qps3 daf Qps3 Qps5 Qps3 Qps4 Qps5 Qps4 Qds Qps4 QTps2 QTps2 Qps3 Qd Qpsc1 Qps4 Qps4 daf Qpsc2 Qps3 daf daf Qps3 Qps4 Qps4 QTps2 Qps5 Qps4 Qps5 daf Qps5 Qps3 Qps4 QTps2 Qps3 Qds daf daf Qps3 Qd daf Qps3 Qps3 Qd Qps4 Qps4 Qa Tps1 Qd daf Qps4 daf daf daf daf daf Qps3 Qps3 daf Qps4 Qps5 Qds Qds Qps4 daf Qps3 Qps4 QTps2 daf daf daf Qd Tps1 Qds daf Qps3 Qps4 Psd Qpsc2 Qds Qpsc2 Qd Qpp5 daf Psg Qps4 Qpp3 Qpsc2 Qps3 Qps3 Qps3 Qds QTps2 Qd Psg Qps5 Qd Qps4 QTpp2 QTps2 Qpp3 daf daf daf Qps4 Qps3 QTps2 Qpp3 Qa Qps3 daf Qps3 Qps3 Qps4 Htd1 Qps5 daf Qps4 daf daf daf Qps5 Qd Qpp3 Qps3 Qps4 Htd2 Qpp3 Qps4 QTpp2 Htd3 daf Htd2 daf Htd3 daf Qpp3 Qpp3 daf Qpp4 Qps5 Qpp4 Qpp4 QTpp2 Qppc2 Qpp4 Qpp5 Htd3 daf daf daf daf daf daf daf Qpp5 Qpp3 Qpp5 Qpp3 Htc2 daf Qppc2 Qpp5 Qpp3 daf Htd2 daf Qpp4 daf Qpp4 Qpp5 Qpp4 Qpp4 Qpp3 Qpp3 Qds Qpp4 Qppc2 Qds Qpp5 Qpp4 Qpp5 Htd4 daf daf Qpp4 Qpp5 Qpp3 Qpp3 Qpp3 Qpp4 Qpp4 Qds Qpp3 Qpp3 daf Qe Qpp4 QTpp2 Qpp4 Qpp4 daf Qpp4 Qds Qd QTpp2 Qpp4 Qpp4 daf Qpp3 QTpp2 Qpp3 daf QTpp2 Qpp3 Qds QTpp2 Qpp3 Qpp3 Tpp1 QTpp2 Qpp4 QTpp2 Qpp3 Qpp4 Qppc2 Qpp3 daf Qpp3 Qd Qpp4 daf QTpp2 Qpp3 Qpp3 Qpp3 daf Qpp4 Qpp3 QTpp2 QTpp2 Qpp4 Qpp3 Qppc2 daf Qpp4 Qpp3 Qpp4 Qpp4 Qpp3 Qpp4 Qpp4 daf Tpp1 QTpp2 Qpp3 Qpp4 Qpp4 Qpp3 Qpp5 Qpp4 Qpp4 Qa Qpp3 Qpp4 Qppc2 QTpp2 Qpp3 Qpp3 Qpp5 Qpp3 daf Qpp4 Qpp4 daf Qppc2 Qpp3 QTpp2 Qpp3 Qpp4 QTpp2 Qpp3 daf Tpp1 Qpp4 daf QTpp2 daf daf Qpp3 Qpp3 daf QTpp2 Qpp3 Qpp3 daf Qpp4 Qpp4 QTpp2 Qpp3 Qds QTpp2 Qpp3 Qpp3 Qpp4 Qpp4 QTpp2 Qpp4 Qpp4 QTpp2 Qpp3 Qpp3 QTpp2 daf Qpp3 Qpp3 Qpp3 daf daf Qpp3 daf Qppc2 Qpp5 Qds daf daf Qpp3 Qpp4 daf daf Qpp4 Qpp3 Qppc2 Qpp3 Qpp4 QTpp2 daf Qpp3 daf QTpp2 Qpp3 Qpp3 Qpp3 Qpp4 Qppc1 Qpp3 Qpp3 QTpp2 Qpp3 Qpp4 QTpp2 Qppc2 Qpp3 QTpp2 daf Qppc2 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 QTpp2 QTpp2 daf QTpp2 Qpp5 Qpp4 daf Qpp3 Qppc2 Qe QTpp2 Qpp3 Qpp3 QTpp2 QTpp2 QTpp2 Qpp4 Qpp4 Qpp5 Qpp4 QTpp2 Qpp5 Qppc1 Qpp3 Qpp4 QTpp2 Qpp3 daf Qpp4 Qpp4 QTpp2 QTpp2 Qot Qpp5 QTpp2 Qpp4 QTpp2 Qpp5 daf Qpp3 Qot Qa daf Qpp4 QTpp2 Qppc2 Qpp3 QTpp2 QTpp2 QTpp2 daf Qpp5 Qpp5 daf Qpp4 Qpp3 Qpp3 Qpp5 QTpp2 daf Qppc2 Qpce Qpce Qe Qpp4 Qppc2 Qpp5 Qpce Qppc2 daf Qpp3 Qpp3 Qpp4 daf Qe Qpp3 QTpp2 Qe Qpp3 Qpp4 Qpp5 Qpp5 Qpp5 Qot Tpp1 Qpp4 Qps3 Qps3 Qps3 Qpp3 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 daf daf daf QTpp2 QTpp2 QTpp2 QTpp2 Qp Qpp3 Qpp3 Qpp3 QTpp2 Qe Qpp4 Qpp4 Qpp4 Qppc1 Qppc1 Qpp4 Qpp4 Qpp5 Qpp5 Qpp4 Qpp3 QTpp2 Qpp3 Qpp4 Qppc2 Qppc2 Qppc2 Qa Qppc2 Qppc2 QTpp2 QTpp2 Qpce daf daf daf daf Qpp3 Qpp3 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 Qpp3 Qpp3 Qpp3 Qppc2 QTpp2 daf Qpp3 daf daf daf daf daf daf Qppc1 Qpp4 Qpp4 Qpp4 daf Qpce Qpp3 Qpp3 QTpp2 QTpp2 Qpp4 Qpp4 Qpp5 Qpp5 Qpp5 Qpp5 Qpp3 Qpp3 Qpp5 Qa Qa Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 daf daf daf daf daf daf daf daf daf daf daf daf Qlt3 Qlt3 Qlt3 Qlt3 Qa Qa Qlt3 Qlt3 Qlt3 Qlt3 Qlt3 daf daf daf Qpp4 Qpp3 Qpp3 Qpp5 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 daf daf daf daf daf daf daf daf daf Qds Qpp3 Qpp3 Qpp3 QTpp2 Qpp3 Qppc2 Qppc2 QTpp2 QTpp2 QTpp2 Qpp3 Qpp5 Qpp5 Qpp3 Qpp4 Qpp4 Qpp4 Qpp3 Qpp3 QTpp2 QTpp2 QTpp2 Qpp4 Qpp4 Qpp5 Qppc1 Qpp3 Qpp3 Qpp3 daf daf daf daf daf daf daf daf daf daf Qpp3 Qpp3 Qd Qd daf daf daf daf Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp4 Qpp4 Qpp5 Qpp5 Qpp4 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 Qpp3 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qa Qa Qa Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 QTpp2 QTpp2 QTpp2 Tpp1 Tpp1 Tpp1 Qpp3 Qpp5 Qpp5 Qpp3 Qpp3 Qpp3 daf daf daf daf daf Qa Qa QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 daf daf daf daf daf daf daf Qd Qd Qpp4 Qpp5 Qpp5 Qpp5 Qpp3 Qpp5 Qpp5 Qpp4 Qpp3 Qpp3 Qpp4 Qpp5 Qppc2 Qppc2 Qppc2 Qppc2 daf daf daf daf daf daf daf daf daf daf daf daf Qd Qd Qd Qd Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qa Qa Qa QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp5 Qpp5 Qpp3 Qpp5 Qpp3 Qpp4 Qpp4 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qds daf daf daf daf daf Qppc2 Qppc2 Qppc2 Qppc2 Qpp3 Qpp3 daf daf daf daf daf daf daf Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp4 Qpp4 Qpp4 Qpp4 Qpp4 Qpp5 Qpp5 Qpp4 QTpp2 Qds Qds Qds daf Qa Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qds Qds Qds Qds daf daf daf daf Qa Qpp5 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp4 Qpp5 Qpp5 Qpp4 Qpp3 Qpp4 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps5 Qps4 Qps4 Qps3 Qpp5 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Htc4 Htc4 Htc3 Htc3 Htc3 Htd3 Htd3 Htc2 Htc2 Htc2 Htc2 Htd2 Htd2 Htd2 Htd2 Htd2 Htd1 Htd1 Htd1 Htd2 Htc1 Htc1 Htc1 Qppc2 Psd Psd Qps3 Qps3 Qps4 Qps4 Qps3 Qpp3 daf daf daf daf Qpp5 Qpp5 Qppc2 Qpp4 Qpp3 Qpp3 Qpp3 Qpp3 Qpp5 Qa Qpp3 Qpp3 Qpp4 Qppc2 Qpp4 Qpp4 daf daf Qps5 Qps5 Qpsc2 Qpp3 Qpp4 Qpp5 Qpsc2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 Qd Qd daf daf daf daf daf daf daf daf daf daf daf Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qpp3 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qppc2 Qpp4 Qpp4 Qpp4 Qpp4 Qpp4 Qpp5 Qpp5 Qpp5 Qpp5 Qps5 Qps5 Qps4 Qps4 Qps4 QTps2 QTps2 Qps3 daf daf daf daf daf QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 QTpp2 Qpp4 Qpp4 Qpp4 Qpp4 Qpp4 Qpp4 Qpp5 Qps5 Qps4 Qps4 Qppc1 Qppc1 Qa Qa Qa Qpp5 daf daf daf daf daf daf Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qa Qa Qa Qa Qpsc2 Qpsc2 Qpsc2 Qpsc2 Tps1 QTps2 QTps2 QTps2 QTps2 QTps2 QTps2 QTps2 Tps1 Tps1 QTps2 QTps2 QTps2 Qpsc2 Qpsc2 Qpsc2 Qps3 Qps3 Qps3 Qps4 Qps4 Qps4 Qps5 Qps4 daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf Qds Qds Qds Qds Qpsc2 Qpsc2 Qpsc2 Tsp1 Qsp3 Qsp3 Qsp4 Qsp4 Qsp3 QTps2 Qps5 Qps5 Qps5 Qps4 Qd Qd Qd Qd Psd Psd Psd Psd Psg Qps4 Qps4 Qps4 Qps5 Qps5 Qps5 Qps5 Qps3 Qps3 Qps2 Qa Qa Qa Qpsc2 Qpsc2 daf daf daf daf daf daf daf daf daf QTps2 QTps2 QTps2 Qps4 Qps3 Qps3 Qps3 Qps5 Qps3 Qps3 Qds Qds Qds Qps5 Qps4 Qpsc1 Qpsc1 Qpsc2 Qpsc2 Qpsc2 Qps5 Qps5 Qps5 Qps5 Qps3 Qps3 Qds daf Qbs Qbs daf Qa Qa Qa Qpsc2 Qpsc2 Qpsc2 Qpsc2 Qpsc2 Qpsc2 Qpsc2 Qps5 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps3 Qps4 Qps4 QTps2 QTps2 Qps4 daf Qds Qds Qds Qps4 Qps4 QTps2 QTps2 Qps4 Qps3 Qps3 Qps4 Tsp1 Qd Qd daf Qps4 Qd Qd Qd Qd Qd daf Qds Qds Qd Qd Qd Qd Qpsc2 Qpsc2 QTps2 daf daf daf daf Psd Psd Psd Psd Psd Psd QTps2 Qpsc2 Qpsc2 Qd Qd Qpsc2 Qpsc2 Qpsc2 Qpsc2 Qpsc2 Qd Qpsc2 daf daf daf daf daf daf daf daf daf daf daf daf daf daf daf Qd Qps3 QTps2 QTps2 QTps2 QTps2 Qps5 Qps5 Qps5 Qps4 Qps4 QTps2 QTps2 QTps2 QTps2 QTps2 QTps2 QTps2 QTps2 Qps5 Qps3 Qps3 Qps3 Qps4 Qps4 Qps3 Qps5 Qa Qa Qps5 8717 10542 9884 10400 11632 9728 8582 10988 10266 8689 8945 8673 8744 8758 9726 9272 9181 9610 9557 9729 9731 9675 9948 12015 9473 3610 000 3610 000 3611 000 3611 000 3612 000 3612 000 3613 000 3613 000 3614 000 3614 000 3615 000 3615 000 3616 000 3616 000 3617 000 3617 000 3618 000 3618 000 3619 000 3619 000 3620 000 3620 000 3621 000 3621 000 3622 000 3622 000 3623 000 3623 000 104°22'30"W 104°22'30"W 104°25'0"W 104°25'0"W 104°27'30"W 104°27'30"W 104°30'0"W 104°30'0"W 32°45'0"N 32°45'0"N 32°42'30"N 32°42'30"N 32°40'0"N 32°40'0"N 32°37'30"N 32°37'30"N 547 000 547 000 548 000 548 000 549 000 549 000 550 000 550 000 551 000 551 000 552 000 552 000 553 000 553 000 554 000 554 000 555 000 555 000 556 000 556 000 557 000 557 000 558 000 558 000 SPRING LAKE ARTESIA HOPE SE LAKE MCMILLAN NORTH PARISH RANCH LAKE MCMILLAN SOUTH SEVEN RIVERS FOSTER RANCH Magnetic Declination May, 2009 8º 15' East At Map Center Base map from U.S. Geological Survey 1955, from photographs taken 1947, Topography by planetable surveys 1955. Polyconic projection, 1927 North American datum, reprojected to UTM projection -- zone 13N 1000-meter Universal Transverse Mercator grid, zone 13, shown in red NEW MEXICO QUADRANGLE LOCATION COMMENTS TO MAP USERS CONTOUR INTERVAL 10 FEET NATIONAL GEODETIC VERTICAL DATUM OF 1929 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). New Mexico Bureau of Geology and Mineral Resources Open-file Geologic Map 160 NEW MEXICO BUREAU OF GEOLOGY AND MINERAL RESOURCES New Mexico Bureau of Geology and Mineral Resources New Mexico Tech 801 Leroy Place Socorro, New Mexico 87801-4796 [505] 835-5490 http://geoinfo.nmt.edu 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 not be the sole source of information for use in locating or designing wells, buildings, roads, or other man-made structures. 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 DIVISION OF NEW MEXICO INSTITUTE OF MINING AND TECHNOLOGY NMBGMR Open-file Geologic Map 160 Last Modified June 2011 1 0 1 0.5 KILOMETER 1000 0 1000 2000 3000 4000 5000 6000 7000 FEET 1 0 1 0.5 MILE 1:24,000 by David J. McCraw and Shannon Williams May 2011 Geologic map of the Dayton quadrangle, Eddy County, New Mexico. New Mexico Bureau of Geology and Mineral Resources, 801 Leroy Place, Socorro, NM 87801 Dayton A A' DESCRIPTION OF MAP UNITS CENOZOIC QUATERNARY and NEOGENE Alluvium, lacustrine, and anthropogenic deposits Disturbed land and/or artificial fill (Historic) — Dumped fill and areas affected by human disturbances, mapped where deposits or extractions are areally extensive. Especially notable are the numerous constructed oil and gas well pads. Also includes the U.S. Bureau of Reclamation’s Kaiser Channel of the Pecos River, as well as other straightened reaches. Quaternary alluvium, undifferentiated (Historic to uppermost Pleistocene) — Brown (7.5YR4/2) to light brown (7.5YR6/3), unconsolidated, moderately sorted, pebbly sand, silt, and clay. Contains primarily carbonate gravels and pebbles. Varies considerably in thickness from <1 to 3 m in tributaries and up to 10-12 m in the floodplain. Pecos River floodplain alluvial backswamp deposits (upper Pleistocene to Historic) — Light reddish-brown (5YR6/4) to very dark gray (7.5YR3/1), unconsolidated, well-sorted, silty sand, sandy clay, and clay in low-lying, poorly drained areas. These areas commonly received only fine-grained, slack-water flood deposition, prior to channelization. Thicknesses range from 3-15 (?) m. Quaternary playa deposits (upper Pleistocene to Holocene) — Pinkish white (7.5YR8/2), unconsolidated, well-sorted, fine-grained sand, silt, and clay Thickness unknown (≥ 1m). Fourmile Draw depression Fourmile Draw formed in the low area between the Rio Peñasco and North Seven Rivers piedmont alluvial complexes, and is utilized in this mapping to differentiate these complex deposits. It is shallowly underlain by Permian Artesia Group sediments that are riddled with collapse depressions and sinkholes. Just west of U.S. Highway 285, it flows into a very large depression, roughly 1-1.5 km wide and 4 km long. This depression likely formed in the uppermost Pleistocene and/or early Holocene. Upon encountering the depression, Fourmile Draw has built 4 fluviodeltaic complexes containing distributary channels and levee deposits (Htc 1-4 and Htd 1-4 , respectively), distinctly mappable from aerial photography. These migrate with time from the western margin to the center of the depression, where the modern Htd 4 complex is located. Youngest Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 1+ m. Youngest Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 1+ m. Younger Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 2 m. Younger Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 2 m. Older Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 2 m. Older Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 2 m. Oldest Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 2 m. Oldest Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 2 m. Pecos Valley alluvial terrace complex 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. On the Dayton quad, much of the higher Rio Peñasco and North Seven Rivers piedmont alluvial complexes are erroneously mapped by Fiedler and Nye (1933) as Blackdom terrace. These materials, however, are all derived from these western tributaries, not the Pecos River. Lakewood terrace alluvial deposits (upper to middle Pleistocene) — Following McCraw, et al. (2007) and McCraw and Land (2008), three distinct, low-lying (upper to uppermost middle(?) Pleistocene) “Lakewood terraces” are recognized. Only the lowest and youngest deposit, Qlt 3 , <1- 2 m above the floodplain, is found on the Dayton quad, extending up the Rio Peñasco. These 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. Stage I pedogenic carbonate, mostly non-gypsiferous. Youngest Lakewood terrace alluvial deposits (upper Pleistocene) — Thickness <1 to 2 m. Orchard Park terrace alluvial deposits (upper Pliocene (?) to upper Pleistocene) — According to Fiedler and Nye (1933), the Orchard Park terrace rises 1-3 m above the Lakewood terrace and 10.5-19 m above the Pecos floodplain. It is comprised of gravels and pebbles of dolomite, limestone, sandstone, chert, and quartzite in a very pale brown (10YR7/4) to reddish brown (5YR4/4), unconsolidated, moderately sorted, coarse- to fine- grained sand, silty sand, silt, and sandy clay. Pedogenic carbonate is a strong stage III. Thickness ranges from 5 to 45 m. Rio Peñasco alluvial piedmont complex Rio Peñasco alluvial piedmont deposits (Upper Pleistocene to Late Miocene(?)) — The headwaters of the Rio Peñasco are located high in the Sacramento Mountains in predominantly carbonate rocks of the San Andres formation (Psa) and clastic sediments of the Yeso formation (Pye). Where it leaves the Permian highlands, it has built a large piedmont alluvial complex, which coalesces with Eagle Creek to the north and the Seven Rivers to the south. These piedmont deposits grade to and onto the Pecos Valley alluvial terraces on the easternmost edge of the Dayton quad. Oldest, highest remnant surfaces (Tpp 1 and QTpp 2 ) are Pliocene or older, and likely graded to a river system which forms Gatuña formation deposits today. Middle to upper Pleistocene piedmont deposits (Qpp 3-4 ) are inset into these and grade to Qot. The youngest, Qpp 5 , grades to Qlt 3 . Several channels (e.g., Tumbleweed Draw) on this piedmont surface were likely former Rio Peñasco channels. Lithologically, the Rio Peñasco piedmont deposits are distinctly different from those of Eagle Creek to the north and Seven Rivers to the south. While gravels are dominated by limestone clasts, dolomite, chert, yellow-brown sandstone, conglomerate, and quartzite are common. The matrix consists of dark yellowish brown (10YR3/4) to light brown (7.5YR6/3), unconsolidated, moderately sorted, coarse- to fine-grained sand, silty sand, silt, and sandy clay. Stage V-VI pedogenic carbonate can be found in the oldest deposits, while middle to upper Pleistocene deposits range from stage IV to III. Degree of pedogenic carbonate development can be the main distinguishing characteristic between the youngest deposits. Youngest Quaternary piedmont alluvium (Holocene to upper Pleistocene) — Thickness 1 to 3 m. Younger Quaternary piedmont alluvium (Upper Pleistocene) — Thickness 2 to 4 m. Old Quaternary piedmont alluvium (Upper to middle Pleistocene) — Most extensive deposit. Thickness 2 to 4 m. Older piedmont alluvium (Middle Pleistocene to late Pliocene) — Thickness 2 to 6 m. Oldest piedmont alluvium (Late Pliocene to late Miocene(?)) — Thickness 2 to 6 m. Rio Peñasco piedmont channel deposits (Historic to upper Pleistocene) — Numerous, thin alluvial channels, swales, and occasional coalescing depression fill deposits drain the piedmont alluvial complex. They usually consist of light brown (7.5YR6/4) to pinkish gray (7.5YR6/2), unconsolidated, poorly sorted, fine-grained sand, silt, and clay sediments. They were often mapped primarily by soil moisture increases in lower areas relative to adjacent piedmont deposits noted on photography. Eolian input often mantles the “v-shaped” contours associated with stream channels and in some areas sand sheets and dunes can fill these channels (Qpce). On the Rio Peñasco, older channels (Qppc 1 ) are mapped on Qpp 4 surfaces, similar and stratigraphically equivalent to those on North Seven Rivers Qps 4 deposits. Young Quaternary piedmont channels (Holocene to upper Pleistocene) — Thickness <1 to 2 m. Older Quaternary piedmont channels (Upper Pleistocene) — Thickness <1 to 2 m. Youngest Quaternary piedmont channels filled with eolian sands, occasionally forming dunes (Holocene to upper Pleistocene) — Thickness ≤ 1 m. North Seven Rivers alluvial piedmont complex North Seven Rivers alluvial piedmont deposits (Upper to middle Pleistocene) — North Seven Rivers, like the other Seven River channels head to the southwest out of the northern Guadelupe Mountains in both San Andres formation (Psa) carbonate rocks and Artesia Group (Queen-Grayburg formations) marine and non-marine redbeds and evaporites. To the south and west of the quad it flows out onto a piedmont alluvial complex, which coalesces with the Rio Peñasco to the north. Oldest, highest remnant surfaces and deposits are correlative to lower Pleistocene to late Miocene (?) piedmont deposits of the Rio Peñasco (Tpp 1 and QTpp 2 ). Like Eagle Creek to the north, gravels are almost exclusively limestone, derived from Psa, supported in a matrix of reddish brown (2.5YR4/6) to light brown (7.5YR6/3), unconsolidated, moderately sorted, coarse- to fine-grained sand, silty sand, silt (largely calcareous), and sandy clay. Topographic expression between the youngest deposits are often subtle to practically non-existent. Distinction is often based upon a stronger developed pedogenic carbonate (Qps 4 = stage III – II+; Qps 5 = stage II). Qps 5 grades to Qlt 3 . Youngest Quaternary piedmont alluvium (Holocene to upper Pleistocene) — Thickness 1 to 3 m. Younger Quaternary piedmont alluvium (Upper Pleistocene) — Thickness 2 to 4 m. Old Quaternary piedmont alluvium (Upper to middle Pleistocene) — Most extensive deposit. Thickness 2 to 4 m. Older piedmont alluvium (Middle Pleistocene to late Pliocene) — Thickness 2 to 6 m. View looking south-southwest of Permian Seven Rivers formation, mixed gypsiferous facies (Psg) gypsum and redbeds in the foreground, Quaternary sinkhole deposits (Qds) in the middle distance, and Permian Seven Rivers dolomite (Psd) at the top of the bluff above Psg beyond the sinkhole. Photo by D. McCraw. REFERENCES Delher, C., Pederson, J., and Wagner, S., 2005, Preliminary geologic map of the Lake McMillan South 7.5 Minute Quadrangle: New Mexico Bureau of Geology and Mineral Resources, Open-File Geologic Map Series, OF-GM 97, 1:24,000. 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. Hawley, J. W., 1993, The Ogallala and Gatuña formations in the southeastern New Mexico Region, a progress report: New Mexico Geological Society Guidebook, 44th Field Conference, p. 261- 269. Kelley, V. C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and Mineral Resources Memoir 24, 78 p. Lyford, F. P., 1973, Valley fill in the Roswell-Artesia area, New Mexico: U.S. Geological Survey Open-file Report 73-163, 26 p. McCraw, D. J., 2008, Preliminary geology of the South Spring Quadrangle, Chaves County, New Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file OF-GM 171, 1:24,000. McCraw, D. J. and Land, L. A., 2008, Preliminary geology of the Lake McMillan North Quadrangle, Eddy County, New Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file OF-GM 167, 1:24,000. McCraw, D. J., Rawling, G., and Land, L. A., 2007, Preliminary geology of the Bitter Lake Quadrangle, Chaves County, New Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file OF-GM 151, 1:24,000. Meinzer, O. E., Reinich, B. C., and Bryan, K., 1926, Geology of No. 3 reservoir at the site of the Carlsbad irrigation project, New Mexico, with respect to water tightness: U.S. Geological Survey Water-supply Paper 580, p. 12-13. Motts, W. S. and Cushman, R. L., 1964, An appraisal of the possibilities of artificial recharge to ground-water supplies in part of the Roswell Basin, New Mexico: U.S. Geological Survey Water-supply Paper 1785, 86 p. Oldest piedmont alluvium (Late Pliocene to late Miocene(?)) — Thickness 2 to 6 m. North Seven Rivers piedmont channel deposits (Historic to upper Pleistocene) — Numerous, thin alluvial channels, swales, and occasional coalescing depression fill deposits drain the piedmont alluvial complex. They usually consist of light brown (7.5YR6/4) to light reddish-brown (5YR6/4), unconsolidated, poorly sorted, fine- grained sand, silt, and clay sediments. They were often mapped primarily by soil moisture increases in lower areas relative to adjacent piedmont deposits noted on photography. Eolian input often mantles the “v-shaped” contours associated with stream channels and in some areas sand sheets and dunes can fill these channels (Qsce). On the North Seven Rivers, older channels (Qpsc 1 ) are mapped on Qps4 surfaces, similar and stratigraphically equivalent to those on Rio Peñasco (Qpp 4 ) deposits. Young Quaternary piedmont channels (Holocene to upper Pleistocene) — Thickness <1 to 2 m. Older Quaternary piedmont channels (Upper Pleistocene) — Thickness <1 to 2 m. Youngest Quaternary piedmont channels filled with eolian sands, occasionally forming dunes (Holocene to upper Pleistocene) — Thickness ≤ 1 m. Quaternary depression fill and sinkhole deposits Quaternary depression fill, undifferentiated (Holocene to middle Pleistocene) — Unconsolidated, well-sorted, fine-grained (fine sands to clay) complexes of alluvial, colluvial, eolian, and occasional lacustrine deposits within closed depressions. Colors variable. Depressions are 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) — Complexes of unconsolidated, well- to poorly-sorted, coarse- to fine-grained sands to clay, alluvial, colluvial, eolian, and occasional lacustrine deposits within closed depressions. Colors variable. Thickness <1 to 3 m. PALEOZOIC Permian Artesia Group Seven Rivers formation, undifferentiated — Cross section only. Queen and Grayburg formations, undifferentiated (Guadelupian) — Cross section only. Lower Permian Formations San Andres formation — Cross section only. Glorieta sandstone tongue — Cross section only. Yeso formation, undifferentiated — Cross section only. Abo formation, undifferentiated — Cross section only. Qa Qbs Qp Qlt3 Qot Qpp5 Qpp4 Qpp3 QTpp2 Tpp1 Qppc2 Qppc1 Qps5 Qpsc2 Htd4 Htd3 Htd2 Htd1 Htc4 Htc3 Htc2 Htc1 Qd Qds Pqg Psr Psa Pg Pye Pa Qpsc1 Qps4 Qps3 QTps2 Tps1 daf Qpce Qpce Qsce GEOLOGIC CROSS SECTION 4,000 ft ASL 3,000’ 2,000’ 1,000’ -1,000’ 0’ SL 4,000 ft ASL 3,000’ 2,000’ 1,000’ -1,000’ 0’ SL 8717 10542 9884 10400 11632 9728 8582 10988 10266 8689 8945 8673 8744 8758 9726 9272 9181 9610 9557 9729 9731 9675 9948 12015 9473 E A’ W A U.S. Highway 285 Bend In Section Rio Peñasco Rio Peñasco Qa Psa Pg Pqg Psr Pye Qa Psa Pg Pa Pqg Pye Qa Psa Pg Pa Pqg Pye Qa Psa Pg Pa Pqg Pye CORRELATION OF MAP UNITS 269 258 250 290 1.8 Ma 780 128 11 0 ka Historic Pleistocene upper lower middle Pliocene Miocene Rio Peñasco piedmont alluvial deposits Neogene Quaternary Seven Rivers Fm Yates Fm Tansill Fm Salado Fm Artesia Group San Andres Fm Yeso Fm Abo Fm Queen- Grayburg Fms Permian Paleozoic 5.3 23.0 Pecos Valley alluvial terrace deposits Depressions and sinkholes P b Holocene Qlt 3 Qot Qd Qds ? ? ? ? Qpp 5 Qpp 4 Qpp 3 QTpp 2 Tpp 1 Qppc 2 Qpce Qppc 1 North Seven Rivers piedmont alluvial deposits Tps 1 Qpsc 2 Qsce Qpsc 1 Qps 5 Qps 4 Qps 3 QTps 2 Alluvial, lacustrine, and fluviodeltaic deposits Qp Htd Htc Qa Qbs A A' 8717 7 EXPLANATION OF MAP SYMBOLS Location of geologic cross section. Geologic contact. Solid where exposed or known, dashed where approximately known, dotted where concealed or inferred. Artesia - Vacuum Arch. Subsurface anticlinal arch warping Permian and older strata. Inclined bedding showing degrees of dip. Arrows showing mean direction of paleoflow, based upon pebble imbrication, n ≥ 20 each arrow. Soil pit. Oil & gas exploration well used in cross section construction.

QUATERNARY and NEOGENE · f f f f f f f f f f f f f f f f f f f f f f f f î o î î " F F F 7 Psd Q d Q d s daf Q ps4 T ps1 P sg p 4 Q d Qps 4 Qp s3 Qps5 Qp 4 Psg daf Qps3 Qp s5

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dafdaf

dafdaf

daf

daf

Qd

Qps3

QTps2

QTps2

QTps2

QTps2

Qps5

Qps5

Qps5

Qps4

Qps4

QTps2

QTps2

QTps2

QTps2

QTps2

QTps2

QTps2

QTps2

Qps5

Qps3

Qps3Qps3

Qps4

Qps4

Qps3Qps5

Qa

Qa

Qps5

8717

105429884

10400

11632

9728

8582

10988

10266

8689

8945

8673

8744

8758

9726

9272

9181 9610 9557

9729

9731

9675

9948

12015

9473

36100003610000

36110003611000

36120003612000

36130003613000

36140003614000

36150003615000

36160003616000

36170003617000

36180003618000

36190003619000

36200003620000

36210003621000

36220003622000

36230003623000

104°22'30"W

104°22'30"W

104°25'0"W

104°25'0"W

104°27'30"W

104°27'30"W

104°30'0"W

104°30'0"W

32°45'0"N 32°45'0"N

32°42'30"N 32°42'30"N

32°40'0"N 32°40'0"N

32°37'30"N 32°37'30"N

547000

547000

548000

548000

549000

549000

550000

550000

551000

551000

552000

552000

553000

553000

554000

554000

555000

555000

556000

556000

557000

557000

558000

558000

SPRINGLAKEARTESIAHOPE SE

LAKEMCMILLAN

NORTHDAYTONPARISH

RANCH

LAKEMCMILLAN

SOUTH

SEVENRIVERS

FOSTERRANCH Magnetic Declination

May, 20098º 15' East

At Map Center

Base map from U.S. Geological Survey 1955, from photographs taken 1947, Topography by planetable surveys 1955.Polyconic projection, 1927 North American datum, reprojected to UTM projection -- zone 13N1000-meter Universal Transverse Mercator grid, zone 13, shown in red

NEW MEXICO

QUADRANGLE LOCATION

COMMENTS TO MAP USERS

CONTOUR INTERVAL 10 FEET

NATIONAL GEODETIC VERTICAL DATUM OF 1929

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).

New Mexico Bureau of Geology and Mineral ResourcesOpen-file Geologic Map 160

NEW MEXICO BUREAU OF GEOLOGY AND MINERAL RESOURCES

New Mexico Bureau of Geology and Mineral ResourcesNew Mexico Tech801 Leroy Place

Socorro, New Mexico87801-4796

[505] 835-5490http://geoinfo.nmt.edu

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 not be the sole source of information for use in locating or designing wells, buildings, roads, or other man-made structures.

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 DIVISION OF NEW MEXICO INSTITUTE OF MINING AND TECHNOLOGY NMBGMR Open-file Geologic Map 160Last Modified June 2011

1 0 10.5 KILOMETER

1000 0 1000 2000 3000 4000 5000 6000 7000 FEET

1 0 10.5 MILE

1:24,000

byDavid J. McCraw and Shannon Williams

May 2011

Geologic map of the Dayton quadrangle,Eddy County, New Mexico.

New Mexico Bureau of Geology and Mineral Resources, 801 Leroy Place, Socorro, NM 87801

Dayton

A

A'

DESCRIPTION OF MAP UNITS

CENOZOIC

QUATERNARY and NEOGENE Alluvium, lacustrine, and anthropogenic deposits

Disturbed land and/or artificial fill (Historic) — Dumped fill and areas affected by human disturbances, mapped where deposits or extractions are areally extensive. Especially notable are the numerous constructed oil and gas well pads. Also includes the U.S. Bureau of Reclamation’s Kaiser Channel of the Pecos River, as well as other straightened reaches.

Quaternary alluvium, undifferentiated (Historic to uppermost Pleistocene) — Brown (7.5YR4/2) to light brown (7.5YR6/3), unconsolidated, moderately sorted, pebbly sand, silt, and clay. Contains primarily carbonate gravels and pebbles. Varies considerably in thickness from <1 to 3 m in tributaries and up to 10-12 m in the floodplain.

Pecos River floodplain alluvial backswamp deposits (upper Pleistocene to Historic) — Light reddish-brown (5YR6/4) to very dark gray (7.5YR3/1), unconsolidated, well-sorted, silty sand, sandy clay, and clay in low-lying, poorly drained areas. These areas commonly received only fine-grained, slack-water flood deposition, prior to channelization. Thicknesses range from 3-15 (?) m.

Quaternary playa deposits (upper Pleistocene to Holocene) — Pinkish white (7.5YR8/2), unconsolidated, well-sorted, fine-grained sand, silt, and clay Thickness unknown (≥ 1m).

Fourmile Draw depression

Fourmile Draw formed in the low area between the Rio Peñasco and North Seven Rivers piedmont alluvial complexes, and is utilized in this mapping to differentiate these complex deposits. It is shallowly underlain by Permian Artesia Group sediments that are riddled with collapse depressions and sinkholes. Just west of U.S. Highway 285, it flows into a very large depression, roughly 1-1.5 km wide and 4 km long. This depression likely formed in the uppermost Pleistocene and/or early Holocene. Upon encountering the depression, Fourmile Draw has built 4 fluviodeltaic complexes containing distributary channels and levee deposits (Htc1-4 and Htd1-4, respectively), distinctly mappable from aerial photography. These migrate with time from the western margin to the center of the depression, where the modern Htd4 complex is located.

Youngest Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 1+ m.

Youngest Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 1+ m.

Younger Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 2 m.

Younger Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 2 m.

Older Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 2 m.

Older Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 2 m.

Oldest Fourmile Draw distributary deposits (Holocene) — Thickness <1 to 2 m.

Oldest Fourmile Draw distributary channel deposits (Holocene) — Thickness <1 to 2 m.

Pecos Valley alluvial terrace complex

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. On the Dayton quad, much of the higher Rio Peñasco and North Seven Rivers piedmont alluvial complexes are erroneously mapped by Fiedler and Nye (1933) as Blackdom terrace. These materials, however, are all derived from these western tributaries, not the Pecos River.

Lakewood terrace alluvial deposits (upper to middle Pleistocene) — Following McCraw, et al. (2007) and McCraw and Land (2008), three distinct, low-lying (upper to uppermost middle(?) Pleistocene) “Lakewood terraces” are recognized. Only the lowest and youngest deposit, Qlt3, <1- 2 m above the floodplain, is found on the Dayton quad, extending up the Rio Peñasco. These 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. Stage I pedogenic carbonate, mostly non-gypsiferous.

Youngest Lakewood terrace alluvial deposits (upper Pleistocene) — Thickness <1 to 2 m.

Orchard Park terrace alluvial deposits (upper Pliocene (?) to upper Pleistocene) — According to Fiedler and Nye (1933), the Orchard Park terrace rises 1-3 m above the Lakewood terrace and 10.5-19 m above the Pecos floodplain. It is comprised of gravels and pebbles of dolomite, limestone, sandstone, chert, and quartzite in a very pale brown (10YR7/4) to reddish brown (5YR4/4), unconsolidated, moderately sorted, coarse- to fine- grained sand, silty sand, silt, and sandy clay. Pedogenic carbonate is a strong stage III. Thickness ranges from 5 to 45 m.

Rio Peñasco alluvial piedmont complex

Rio Peñasco alluvial piedmont deposits (Upper Pleistocene to Late Miocene(?)) — The headwaters of the Rio Peñasco are located high in the Sacramento Mountains in predominantly carbonate rocks of the San Andres formation (Psa) and clastic sediments of the Yeso formation (Pye). Where it leaves the Permian highlands, it has built a large piedmont alluvial complex, which coalesces with Eagle Creek to the north and the Seven Rivers to the south. These piedmont deposits grade to and onto the Pecos Valley alluvial terraces on the easternmost edge of the Dayton quad. Oldest, highest remnant surfaces (Tpp1 and QTpp2) are Pliocene or older, and likely graded to a river system which forms Gatuña formation deposits today. Middle to upper Pleistocene piedmont deposits (Qpp3-4) are inset into these and grade to Qot. The youngest, Qpp5, grades to Qlt3. Several channels (e.g., Tumbleweed Draw) on this piedmont surface were likely former Rio Peñasco channels.

Lithologically, the Rio Peñasco piedmont deposits are distinctly different from those of Eagle Creek to the north and Seven Rivers to the south. While gravels are dominated by limestone clasts, dolomite, chert, yellow-brown sandstone, conglomerate, and quartzite are common. The matrix consists of dark yellowish brown (10YR3/4) to light brown (7.5YR6/3), unconsolidated, moderately sorted, coarse- to fine-grained sand, silty sand, silt, and sandy clay. Stage V-VI pedogenic carbonate can be found in the oldest deposits, while middle to upper Pleistocene deposits range from stage IV to III. Degree of pedogenic carbonate development can be the main distinguishing characteristic between the youngest deposits.

Youngest Quaternary piedmont alluvium (Holocene to upper Pleistocene) — Thickness 1 to 3 m.

Younger Quaternary piedmont alluvium (Upper Pleistocene) — Thickness 2 to 4 m.

Old Quaternary piedmont alluvium (Upper to middle Pleistocene) — Most extensive deposit. Thickness 2 to 4 m.

Older piedmont alluvium (Middle Pleistocene to late Pliocene) — Thickness 2 to 6 m.

Oldest piedmont alluvium (Late Pliocene to late Miocene(?)) — Thickness 2 to 6 m.

Rio Peñasco piedmont channel deposits (Historic to upper Pleistocene) — Numerous, thin alluvial channels, swales, and occasional coalescing depression fill deposits drain the piedmont alluvial complex. They usually consist of light brown (7.5YR6/4) to pinkish gray (7.5YR6/2), unconsolidated, poorly sorted, fine-grained sand, silt, and clay sediments. They were often mapped primarily by soil moisture increases in lower areas relative to adjacent piedmont deposits noted on photography. Eolian input often mantles the “v-shaped” contours associated with stream channels and in some areas sand sheets and dunes can fill these channels (Qpce). On the Rio Peñasco, older channels (Qppc1) are mapped on Qpp4 surfaces, similar and stratigraphically equivalent to those on North Seven Rivers Qps4 deposits.

Young Quaternary piedmont channels (Holocene to upper Pleistocene) — Thickness <1 to 2 m.

Older Quaternary piedmont channels (Upper Pleistocene) — Thickness <1 to 2 m.

Youngest Quaternary piedmont channels filled with eolian sands, occasionally forming dunes (Holocene to upper Pleistocene) — Thickness ≤ 1 m.

North Seven Rivers alluvial piedmont complex

North Seven Rivers alluvial piedmont deposits (Upper to middle Pleistocene) — North Seven Rivers, like the other Seven River channels head to the southwest out of the northern Guadelupe Mountains in both San Andres formation (Psa) carbonate rocks and Artesia Group (Queen-Grayburg formations) marine and non-marine redbeds and evaporites. To the south and west of the quad it flows out onto a piedmont alluvial complex, which coalesces with the Rio Peñasco to the north. Oldest, highest remnant surfaces and deposits are correlative to lower Pleistocene to late Miocene (?) piedmont deposits of the Rio Peñasco (Tpp1 and QTpp2). Like Eagle Creek to the north, gravels are almost exclusively limestone, derived from Psa, supported in a matrix of reddish brown (2.5YR4/6) to light brown (7.5YR6/3), unconsolidated, moderately sorted, coarse- to fine-grained sand, silty sand, silt (largely calcareous), and sandy clay. Topographic expression between the youngest deposits are often subtle to practically non-existent. Distinction is often based upon a stronger developed pedogenic carbonate (Qps4= stage III – II+; Qps5 = stage II). Qps5 grades to Qlt3.

Youngest Quaternary piedmont alluvium (Holocene to upper Pleistocene) — Thickness 1 to 3 m.

Younger Quaternary piedmont alluvium (Upper Pleistocene) — Thickness 2 to 4 m.

Old Quaternary piedmont alluvium (Upper to middle Pleistocene) — Most extensive deposit. Thickness 2 to 4 m.

Older piedmont alluvium (Middle Pleistocene to late Pliocene) — Thickness 2 to 6 m.

View looking south-southwest of Permian Seven Rivers formation, mixed gypsiferous facies (Psg) gypsum and redbeds in the foreground, Quaternary sinkhole deposits (Qds) in the middle distance, and Permian Seven Rivers dolomite (Psd) at the top of the bluff above Psg beyond the sinkhole. Photo by D. McCraw.

REFERENCES

Delher, C., Pederson, J., and Wagner, S., 2005, Preliminary geologic map of the Lake McMillan South 7.5 Minute Quadrangle: New Mexico Bureau of Geology and Mineral Resources, Open-File Geologic Map Series, OF-GM 97, 1:24,000.

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.

Hawley, J. W., 1993, The Ogallala and Gatuña formations in the southeastern New Mexico Region, a progress report: New Mexico Geological Society Guidebook, 44th Field Conference, p. 261- 269.

Kelley, V. C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and Mineral Resources Memoir 24, 78 p.

Lyford, F. P., 1973, Valley fill in the Roswell-Artesia area, New Mexico: U.S. Geological Survey Open-file Report 73-163, 26 p.

McCraw, D. J., 2008, Preliminary geology of the South Spring Quadrangle, Chaves County, New Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file OF-GM 171, 1:24,000.

McCraw, D. J. and Land, L. A., 2008, Preliminary geology of the Lake McMillan North Quadrangle, Eddy County, New Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file OF-GM 167, 1:24,000.

McCraw, D. J., Rawling, G., and Land, L. A., 2007, Preliminary geology of the Bitter Lake Quadrangle, Chaves County, New Mexico: N.M. Bureau of Geology and Mineral Resources, Open-file OF-GM 151, 1:24,000.

Meinzer, O. E., Reinich, B. C., and Bryan, K., 1926, Geology of No. 3 reservoir at the site of the Carlsbad irrigation project, New Mexico, with respect to water tightness: U.S. Geological Survey Water-supply Paper 580, p. 12-13.

Motts, W. S. and Cushman, R. L., 1964, An appraisal of the possibilities of artificial recharge to ground-water supplies in part of the Roswell Basin, New Mexico: U.S. Geological Survey Water-supply Paper 1785, 86 p.

Oldest piedmont alluvium (Late Pliocene to late Miocene(?)) — Thickness 2 to 6 m.

North Seven Rivers piedmont channel deposits (Historic to upper Pleistocene) — Numerous, thin alluvial channels, swales, and occasional coalescing depression fill deposits drain the piedmont alluvial complex. They usually consist of light brown (7.5YR6/4) to light reddish-brown (5YR6/4), unconsolidated, poorly sorted, fine-grained sand, silt, and clay sediments. They were often mapped primarily by soil moisture increases in lower areas relative to adjacent piedmont deposits noted on photography. Eolian input often mantles the “v-shaped” contours associated with stream channels and in some areas sand sheets and dunes can fill these channels (Qsce). On the North Seven Rivers, older channels (Qpsc1) are mapped on Qps4 surfaces, similar and stratigraphically equivalent to those on Rio Peñasco (Qpp4) deposits.

Young Quaternary piedmont channels (Holocene to upper Pleistocene) — Thickness <1 to 2 m.

Older Quaternary piedmont channels (Upper Pleistocene) — Thickness <1 to 2 m.

Youngest Quaternary piedmont channels filled with eolian sands, occasionally forming dunes (Holocene to upper Pleistocene) — Thickness ≤ 1 m.

Quaternary depression fill and sinkhole deposits

Quaternary depression fill, undifferentiated (Holocene to middle Pleistocene) — Unconsolidated, well-sorted, fine-grained (fine sands to clay) complexes of alluvial, colluvial, eolian, and occasional lacustrine deposits within closed depressions. Colors variable. Depressions are 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) — Complexes of unconsolidated, well- to poorly-sorted, coarse- to fine-grained sands to clay, alluvial, colluvial, eolian, and occasional lacustrine deposits within closed depressions. Colors variable. Thickness <1 to 3 m.

PALEOZOIC

Permian Artesia Group

Seven Rivers formation, undifferentiated — Cross section only.

Queen and Grayburg formations, undifferentiated (Guadelupian) — Cross section only.

Lower Permian Formations

San Andres formation — Cross section only.

Glorieta sandstone tongue — Cross section only.

Yeso formation, undifferentiated — Cross section only.

Abo formation, undifferentiated — Cross section only.

Qa

Qbs

Qp

Qlt3

Qot

Qpp5

Qpp4

Qpp3

QTpp2

Tpp1

Qppc2

Qppc1

Qps5

Qpsc2

Htd4

Htd3

Htd2

Htd1

Htc4

Htc3

Htc2

Htc1

Qd

Qds

Pqg

Psr

Psa

Pg

Pye

Pa

Qpsc1

Qps4

Qps3

QTps2

Tps1

daf

QpceQpce

Qsce

GEOLOGIC CROSS SECTION

4,000 ft ASL

3,000’

2,000’

1,000’

-1,000’

0’ SL

4,000 ft ASL

3,000’

2,000’

1,000’

-1,000’

0’ SL

8717

1054

2

9884

1040

0

1163

2

9728

8582

1098

8

1026

6

8689

8945

8673

8744

8758

9726

9272

9181

9610

9557

9729

9731

9675

9948

1201

5

9473

EA’

WA

U.S. Highway285

Bend InSection

Rio

Peñ

asco

Rio

Peñ

asco

Qa

Psa

Pg

Pqg

Psr

Pye

Qa

Psa

Pg

Pa

Pqg

Pye

Qa

Psa

Pg

Pa

Pqg

Pye

Qa

Psa

Pg

Pa

Pqg

Pye

CORRELATION OF MAP UNITS

269

258

250

290

1.8 Ma

780

128

11

0 kaHistoric

Ple

isto

cene

uppe

rlo

wer

mid

dle

Plio

cene

Mio

cene

Rio Peñasco piedmont alluvial deposits

Neo

gene

Qua

tern

ary

Seve

nRi

vers

FmYa

tes FmTa

nsill

FmSa

lado

Fm

Artes

ia G

roup

San A

ndre

sFm

Yeso

FmAb

oFm

Que

en-

Gra

ybur

g Fm

s

Per

mia

n

Pal

eozo

ic

5.3

23.0

Pecos Valley alluvial terrace deposits

Depressions andsinkholes

Permian bedrock

Holocene

Qlt3

Qot

PsrPsg

Psd

Pqg

Psa

Pye

Py

Ps

Pa

PtPtm

Ptd

Qd Qds

?

??

?

Qpp5

Qpp4

Qpp3

QTpp2

Tpp1

Qppc2 QpceQppc1

North Seven Rivers piedmont alluvial deposits

Tps1

Qpsc2 QsceQpsc1

Qps5

Qps4

Qps3

QTps2

Alluvial, lacustrine, and fluviodeltaic deposits

Qp

Htd Htc

Qa Qbs

A A'

8717

7

EXPLANATION OF MAP SYMBOLS

Location of geologic cross section.

Geologic contact. Solid where exposed or known, dashed where approximately known, dotted where concealed or inferred.

Artesia - Vacuum Arch. Subsurface anticlinal arch warping Permian and older strata.

Inclined bedding showing degrees of dip.

Arrows showing mean direction of paleoflow, based upon pebble imbrication, n ≥ 20 each arrow.

Soil pit.

Oil & gas exploration well used in cross section construction.

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