the surface water system. Snow melt in the high VOLCANIC STRATIGRAPHY OF THE WEST- mountains recharges shallow perched aquifers ERN SIERRA BLANCA VOLCANIC FIELD, Abstracts that discharge at springs that feed streams and SOUTH-CENTRAL NEW MEXICO, S. A. Kel- ponds where evaporation occurs. Water in ponds ley, [email protected], and D. J. Koning, and streams may then recharge another shallow New Mexico Bureau of Geology and Mineral perched aquifer, which again may discharge at a Resources, New Mexico Institute of Mining and spring at a lower elevation. This cycle may occur Technology, Socorro, New Mexico 87801; K. A. New Mexico Geological Society several times until the water is deep enough to be Kempter, 2623 Via Caballero del Norte, Santa Fe, spring meeting isolated from the surface water system. A deeper New Mexico 87505; K. E. Zeigler, Zeigler Geo- regional aquifer may exist in this area. East of logic Consulting, Albuquerque, New Mexico The New Mexico Geological Society annual Mayhill along the Pecos Slope, regional ground 87123; L. Peters, New Mexico Bureau of Geology spring meeting was held on April 16, 2010, at the water flow is dominantly to the east toward the and Mineral Resources, New Mexico Institute of Mining and Technology, Socorro, New Mex- Macey Center, New Mexico Tech, Socorro. Fol- Roswell Artesian Basin. Some ground water also ico 87801; and F. Goff, Department of Earth and lowing are the abstracts from all sessions given flows to the southeast toward the Salt Basin and to the west into the Tularosa Basin. Planetary Sciences, University of New Mexico, at that meeting. Albuquerque, New Mexico 87131 Keynote presentation p. 60 session 1—geology of the sacramento A thick succession of trachyandesite, trachydacite, volcaniclastic sediments, and minor welded ash- Session 1—Geology of the Sacramento Mountains Mountains and Tularosa Basin and Tularosa Basin p. 60 flow tuffs is preserved on three north-south-strik- Session 2—Spring microbes and caves p. 60 COMPARISON OF ALLUVIAL FAN GEO- ing fault blocks on the west side of Sierra Blanca. Session 3—Hydrogeology of the Sacramento MORPHOLOGY, SEDIMENTATION, AND The volcanic rocks on the eastern fault block, Mountains p. 61 EROSION ALONG THE EASTERN MARGIN which includes Sierra Blanca, are composed of Session 4—Paleontology p. 63 OF THE TULAROSA BASIN, NEW MEXICO, a basal thick (> 250 m) sequence of pyroxene- Session 5—Magmatism and volcanism p. 63 D. J. Koning, [email protected], New Mexico phyric trachyandesite breccia and debris-flow deposits overlain by a stack of plagioclase-phyric Session 6—Climate p. 64 Bureau of Geology and Mineral Resources, trachyandesite lava flows that are variably fine Session 7—Stratigraphy p. 64 New Mexico Institute of Mining and Technol- grained to crystal rich. The trachyandesite flows, Session 8—Hydrology p. 65 ogy, Socorro, New Mexico 87801 40 39 Poster sessions with published Ar/ Ar ages of 29.3–37.3 Ma, This study compares two sets of alluvial fans are among the oldest volcanic rocks in the area. Paleontology and stratigraphy p. 65 along the eastern margin of the Tularosa Basin. Volcaniclastic sediments are not common in the Granite and rock piles p. 68 Alluvial fans of the first set are gravelly and con- stacked lava flow section, but are preserved in Hydrogeology p. 69 tain both debris-flow and stream-flow sediment. paleochannels cut in the upper part of the plagio- Geophysics and structure p. 69 Fan-head trenching is confined adjacent to the clase-phyric trachyandesite. The volcanic rocks Alluvial fans and travertine deposits p. 70 mountain front. Fans belonging to the second set in the middle fault block between Sierra Blanca Geologic mapping and spatial archeology p. 71 are derived from large mountain front drainages and the Godfrey Hills are primarily the pyroxene- Author and subject indices p. 72 north of Alamogordo. These alluvial fans lack phyric trachyandesite breccia. debris-flow sediment, have less gravel and more The western fault block, including the Godfrey Keynote clay, and exhibit entrenched, main-stem arroyos Hills, exposes the younger part of the volcanic suc- throughout their length. The longer arroyos per- cession of the Sierra Blanca volcanic field. The old- HYDROGEOLOGY OF THE SOUTHERN haps relate to their finer-grained sediment and est flows, found at low elevation on the south and SACRAMENTO MOUNTAINS, G. C. Rawl- higher discharges from their respective moun- west sides of the Godfrey Hills, are dark-colored, ing, [email protected], New Mexico Bureau of tain front canyons. porphyritic trachyandesite similar to the plagio- Geology and Mineral Resources–Albuquerque Both sets of alluvial fans experienced simi- clase-phyric trachyandesite on Sierra Blanca. Volca- Office, New Mexico Institute of Mining and lar erosional and depositional histories in niclastic channel fills are locally present between Technology, Albuquerque, New Mexico 87106 their proximal and medial areas. Erosion was these flows. The dark-colored porphyritic tra- The southern Sacramento Mountains are an impor- concentrated in arroyos during 18–8 ka, with chyandesite flows are thinner and the volcani- tant source of recharge to the lower Pecos Valley, pedogenesis occurring on surfaces between clastic sedimentary rocks are thicker toward the Roswell Artesian Basin, and Salt Basin aquifers. arroyos. Widespread aggradation occurred north end of the hills. The dark-colored flows are overlain by (1) a discontinuous fine-grained, flow- Significant declines in water levels in wells, spring between 8 and 3 ka on both sets of fans. On the banded trachyte, (2) a thick volcaniclastic interval and stream flow have occurred in the past 15 yrs. first set of alluvial fans, stream-flow sediment containing a few thin, discontinuous trachyandes- In response, the Otero Soil and Water Conserva- commonly transitions upward into debris-flow ite and trachydacite flows capped by a continu- tion District and the New Mexico Bureau of Geol- sediment, with an inset, coarse-grained deposit ous trachyandesite flow, (3) a welded ash-flow ogy and Mineral Resources (NMBGMR) initiated found below the debris flows. Stream-flow and clayey-sandy sheetflood deposits characterize tuff (Palisades tuff; 28.67± 0.05 Ma), (4) a sparsely a multi-scale study of the regional hydrogeology porphyritic trachyandesite with zones of breccia to delineate areas and timing of ground water the second set of alluvial fans between 8 and 3 ka. Coarse-grained channel-fill deposits inter- (28.59 ± 0.07 Ma), and (5) an upper fine-grained recharge, determine direction and rates of ground finger with clayey-silty, very fine to medium- trachyte. The Palisades tuff is thicker at the north water movement, and understand interactions grained sand. Fine-grained sediment is gener- end of the Godfrey Hills. In addition, a thin tuff between different aquifers and the ground water ally bioturbated, internally massive, and has (tuff of Bucky Pasture) is preserved in the volca- and surface water systems in the mountains. undergone weak pedogenesis. Pebbles in the niclastic interval in the northern Godfrey Hills. The Yeso Formation, which consists of layers of fine-grained sediment are scattered or in thin Thickness variations and the degree of welding limestone, dolomite, sandstone, and siltstone, is the to medium lenses. These observations indicate of the tuffs suggest the presence of an undetected primary aquifer in the study area. Fractured lime- an aggrading fan landscape during the middle local caldera northeast of the Godfrey Hills. stones and dolomites are the main source of water Holocene. Erosion occurred between 3 and 2 ka for most springs and wells in the southern Sacra- on both sets of alluvial fans. Another episode of session 2—Spring microbes and caves mento Mountains. Recharge primarily occurs in the aggradation occurred during 0.5–2.0 ka, which high mountains west of Mayhill, where the Yeso on the second fan set is marked by better strati- MICROBIAL RICHNESS AND DIVERSITY Formation is exposed at the surface. Stable isotope fication and slightly coarser texture than earlier IN CO2-RICH MOUND SPRINGS OF THE data suggest that snow melt usually contributes Holocene deposits. North of Alamogordo, there TIERRA AMARILLA ANTICLINE, NEW MEX- significantly more to ground water recharge than was eolian reworking of sediment and local- ICO, B. Cron, [email protected], and L. J. Crossey, summer precipitation. However, extreme summer ized, periodic arroyo formation and backfilling Department of Earth and Planetary Sciences, Uni- precipitation events, such as those that occurred during 0.5–2.0 ka. These observations indicate versity of New Mexico, Albuquerque, New Mex- in 2006 and 2008 do recharge the ground water that the late Holocene experienced episodes of ico 87131; D. E. Northup, Department of Biology, system, resulting in significant increases in water surface instability, perhaps due, at least in part, University of New Mexico, Albuquerque, New levels in wells and spring discharge. to sparser grass and low-lying shrubs. Pro- Mexico 87131; and K. E. Karlstrom, Department of The ground water system in the high moun- nounced erosion has occurred on the proximal Earth and Planetary Sciences, University of New tains west of Mayhill is characterized by several and medial parts of both alluvial fan sets dur- Mexico, Albuquerque, New Mexico 87131 fracture-controlled leaky perched aquifers that are ing the past 100–150 yrs, resulting in prevalent A series of mesothermal (~ 25° C) mound springs interconnected by regional fracture networks and gravel lag deposits and gully dissection. located along the Tierra Amarilla (TA) anticline are

60 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 related to a regional occurrence of CO2-rich traver- only b.p. 836 yrs, indicating an abrupt change 87801; G. C. Rawling, New Mexico Bureau of Geol- tine-depositing springs in north-central New Mex- in climatic or hydrochemical conditions within ogy and Mineral Resources–Albuquerque Office, ico. Previous work has shown that these springs the past millennium. The Snowy River passage New Mexico Institute of Mining and Technology, 3 4 3 exhibit geochemical ( He/ He and CO2/ He) evi- has been intermittently flooded for the past 2 yrs Albuquerque, New Mexico 87106; S. S. Timmons, dence for the presence of endogenic fluids. We have during the Southwest monsoon season, during and T. Kludt, New Mexico Bureau of Geology and hypothesized that CO2-rich mound springs such as which a thin film of new calcite was deposited. Mineral Resources, New Mexico Institute of Min- TA exhibit tectonic, geochemical, and microbiologi- The source of water in the passage is unknown. ing and Technology, Socorro, New Mexico 87801 cal similarities to marine vent systems. To assess Water level data loggers show abrupt disap- Ground water flow in the southern Sacramento the geochemistry and the metabolic reactions in pearance of floodwaters during winter months Mountains is related to regional fracture systems these springs on a real-time basis, we deployed when the monsoonal rains are over, suggesting a within the highly heterogeneous Yeso Formation. multi-parameter sondes at various depths in two point source of recharge to the cave system via a As a part of the Sacramento Mountains hydroge- springs on the axis of the anticline. Continuous sinkhole or losing stream, and possibly an as yet ology study, water from precipitation, streams, measurements of pH, temperature, conductivity, undiscovered second entrance to the south. springs, and wells was sampled and analyzed dissolved oxygen, and depth were collected every for the stable isotopes of oxygen and hydrogen. five minutes for five days. The temperature and Stable isotope data for precipitation were used pH results indicate a weak diurnal signal at ~ 1 m session 3—hydrogeology of to develop a local meteoric water line (LMWL). depth at the higher-discharge spring. The data the sacramento mountains Seasonal fluctuations along the LMWL define from ~ 6 m depth from the same spring displayed expected isotopic compositions for summer and invariant temperature at ~ 26° C, pH 6, and anaero- IDENTIFICATION OF A REGIONAL PER- winter precipitation. An elevation effect was bic conditions. We use established protocols from CHED GROUND WATER SYSTEM IN THE observed for summer precipitation but not for studies for geochemical modeling to assess ener- SOUTHERN SACRAMENTO MOUNTAINS, winter precipitation. Over the 3 yrs that precipi- getics in extreme environments. We use denaturing OTERO COUNTY, NEW MEXICO, S. T. Finch, tation was collected, the Sacramento Mountains gradient gel electrophoresis (DGGE) to determine [email protected], John Shomaker & Asso- experienced two discrete recharge events due to whether the mesothermal springs have similar ciates, Inc., Water-Resource and Environmen- above average precipitation during the summers species composition to hydrothermal vents. Envi- tal Consultants, 2611 Broadbent Parkway NE, of 2006 and 2008. These recharge events resulted ronmental samples were collected on 0.22 microm- Albuquerque, New Mexico 87107 in an increase in ground water levels over most of the study area. eter Millipore Sterivex filters from several springs The southern Sacramento Mountains, defined and preserved in sucrose lysis buffer. DGGE bands Stable isotope data for spring and well water in this study as the mountains south of US–70 in the high mountains indicate a dual porosity were sequenced from mud and filtered DNA to Otero Mesa, are dominated by a 40-mi long, system. The isotopic compositions of water in extracts. These samples were found to be signifi- north-south-trending crest with an average eleva- the mobile hydrologic system, which is associ- cantly similar to marine organisms (> 94%). DNA tion of 8,000 ft amsl. The Sacramento Mountain ated with fractured limestone and dolomite, was found to be 94% similar to Zetaproteobacteria crest is capped with Permian-age sediments of plot along an evaporation line (slope ~ 5.5) that that are also found in the deep-sea hydrothermal the San Andres Limestone and Yeso Formation, region of the East Lau Spreading Center and uncul- and these sedimentary rocks slope gradually to intersects the LMWL in the range of expected tured environmental bacterial samples collected the east toward the Pecos River approximately winter values. This trend suggests that the pri- from seamounts located along the Kermadec Arc 80 mi away. Water resources of the Sacramento mary source of ground water recharge is snow- (96% similarity). Algoriphagus sp. LYX05, an organ- Mountains have been studied extensively over melt that undergoes mixing and evaporation in ism isolated from sediment along the coastal region the past several decades, particularly in the fractures and mountain streams. The isotopic of the Yellow Sea, was the closest relative to clones developed areas of Ruidoso, Cloudcroft, and compositions of water in immobile regions, which obtained from another spring (97% similarity). Timberon, New Mexico. Two common themes are probably located in nonfractured portions or smaller fractures within the Yeso Formation, plot These data support the hypothesis that CO -rich have emerged from these studies: (1) most 2 along the LMWL and appear to be controlled by springs in terrestrial extensional settings have simi- springs in the Sacramento Mountains occur at the the elevation of local precipitation. larities to marine vents and offer rich potential for San Andres–Yeso contact, and (2) the San Andres The isotopic composition of most springs sam- linking mantle fluids to near-surface hydrochemis- Limestone and Yeso Formation are considered as pled approximately one month after the 2006 try and unique microbial niches. a regional aquifer hydraulically connected. Results from deep well drilling at Cloudcroft monsoon season plotted near the LMWL. Tritium demonstrate the primary ground water system is and water chemistry data indicate that most of this THE SNOWY RIVER FORMATION IN FORT perched in the San Andres Limestone and under- water was not derived from 2006 monsoons. The STANTON CAVE, New Mexico: NEW lying limestone beds in the upper Yeso Formation. isotopic compositions of spring waters changed RESULTS FROM RADIOMETRIC DATING Near the crest, the strata underlying this regional with time over the next 18 months, shifting AND HYDROLOGIC OBSERVATIONS OF perched ground water system are largely unsatu- away from the LMWL, until they plotted along THE WORLD’S LONGEST SPELEOTHEM, rated with localized pockets of saline ground water. the evaporation line. Then the isotopic composi- tion of spring waters began to shift again toward L. Land, [email protected], New Mexico The lateral extent of this regional perched ground the LMWL shortly after the precipitation events Bureau of Geology and Mineral Resources, and water system has been defined by ground water in 2008. We interpret the isotopic shift toward the National Cave and Karst Research Institute, elevation and water chemistry data. Farther east of the LMWL as a result of immobile waters being New Mexico Institute of Mining and Technol- the crest and downslope, the strata underlying the flushed into the mobile hydrologic system due to ogy, 1400 Commerce Drive, Carlsbad, New regional perched ground water system contain a these extreme summer precipitation events. Mexico 88220; V. Polyak, Department of Earth regional ground water system approximately 200 ft and Planetary Sciences, University of New lower in elevation and characterized by older water Mexico, Albuquerque, New Mexico 87131; and with chemistry different than the perched system. WATER CHEMISTRY TRENDS FROM WELLS B. T. Newton, Mexico Bureau of Geology and The regional perched ground water system in the AND SPRINGS IN THE SOUTHERN SAC- Mineral Resources, New Mexico Institute of southern Sacramento Mountains covers approxi- RAMENTO MOUNTAINS, NEW MEXICO, Mining and Technology, Socorro, New Mexico mately 300 mi2 from Cloudcroft to Timberon, and S. S. Timmons, [email protected], and B. T. 87801 is defined by ground water elevation contours Newton, New Mexico Bureau of Geology and greater than 6,600 ft amsl. This perched ground The Snowy River formation, a pool deposit Mineral Resources, New Mexico Institute of water system is the primary source for springs located in a recently discovered passage in Fort Mining and Technology, Socorro, New Mex- Stanton Cave, New Mexico, may be the world’s and perennial streams in the southern Sacramento ico 87801; and F. K. Partey, AMEC Earth and longest continuous cave deposit. The formation Mountains, and recharge to the Pecos Slope. Environmental, PMB Airport Post office, East is composed of tufa-like white coralloid calcite Legon, ACCRA, Ghana lining an old subsurface stream channel, and THE STABLE ISOTOPIC COMPOSITIONS As part of the southern Sacramento Mountains currently extends from north to south for > 7 km OF NATURAL WATERS IN THE SOUTH- hydrogeology study, funded by the Otero Soil with its southern terminus still undefined. Core ERN SACRAMENTO MOUNTAINS, New and Water Conservation District, the New Mexi- samples collected from the Snowy River deposit Mexico: IMPLICATIONS FOR CLIMATIC co Bureau of Geology and Mineral Resources has reveal a laminated internal structure, indicating AND HYDROGEOLOGIC CONTROLS ON sampled 42 springs and 77 wells for ion chemis- episodic deposition of sub-millimeter scale cal- GROUND WATER RECHARGE, B. T. Newton, try and trace metals, as well as other constitu- cite laminae during periods when the passage [email protected], New Mexico Bureau of Geol- ents. Overall, spring and well samples indicate is flooded by CaCO3-saturated water. The basal ogy and Mineral Resources, New Mexico Institute that ground water is dominated by calcium and layer has been dated with U-Th techniques at of Mining and Technology, Socorro, New Mexico magnesium as the cations and bicarbonate and

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 61 sulfate as the main anions. These results support most common species. Thinning slated to begin four wells. It is likely that the four wells are tap- that carbonate dissolution is the dominant chem- in fall 2010 will reduce the average tree density to ping four different saturated water-bearing zones. ical process influencing the water chemistry. 40–60 trees/acre. The relatively shallow water-bearing zones found Springs, located mostly within the high moun- Well logs from three observation wells were at the higher elevation wells probably represent tains region of the study area, are typically cool used to characterize the subsurface geology. different perched aquifer systems at different waters (on average 10° C) and are dominantly cal- Measurements begun in mid-2008 include field stratigraphic levels. The deeper ground water cium-bicarbonate or calcium-magnesium bicar- surveys, soil and water chemistry analyses, and encountered in the lowest elevation well may bonate water types. Springs found in the north- automated sensor data. Automated data collected represent a more regional aquifer system. ern regions of the study area have higher TDS from multiple sites include: spring discharge, and concentrations of sulfate, chloride, strontium, valley ground water levels, soil moisture, matric sodium, magnesium, and silica. potential, canopy throughfall, and precipitation PLOT-SCALE SOIL WATER FLUX AND RUN- Well water samples, which were collected from and climate data. OFF IN A MIXED CONIFER FOREST IN THE sites over a larger region, have higher specific Well logs, ground water level data, and geo- SACRAMENTO MOUNTAINS, New Mex- conductance and higher ion concentrations, in chemical data indicate a complex multi-layered ico, H. Garduño, and A. Fernald, Animal and general, compared to springs. Also, well water ground water system. Chloride and stable isotope Range Sciences Department, New Mexico State temperatures are warmer than springs at an profiles in soils suggest rapid movement of water University, Las Cruces, New Mexico, 88003; average of 15.4° C. About 32% of the well water through the thin rocky soils, indicating high infil- M. Shukla, Plant and Environmental Sciences types are calcium-bicarbonate or calcium-mag- tration rates and low runoff. Spring hydrographs, Department, New Mexico State University, nesium bicarbonate (similar to springs), but also stable isotope data, and water chemistry suggest Las Cruces, New Mexico 88003; B. T. Newton, have slightly more “evolved” water types, with that discharge from the two springs largely comes New Mexico Bureau of Geology and Mineral about 65% calcium-magnesium bicarbonate-sul- from outside of the watershed and are therefore Resources, New Mexico Institute of Mining and fate, or sulfate-bicarbonate water types. Similar considered to be inputs. Other inputs include Technology, Socorro, New Mexico 87801; and to springs, well water samples show increases local precipitation and inflowing ground water. D. Vanleeuwen, Department of Economics and in ion concentrations toward the north, but the Outputs include evapotranspiration, and both International Business, New Mexico State Uni- dominant increases are found toward the east. shallow and deep ground water flow. versity, Las Cruces, New Mexico 88003 The trends of our water chemistry, with some ground water ages, suggest regional ground Mechanical thinning effects in forested stands water flow paths exist, despite multiple perched EFFECTS OF LATERAL AND VERTICAL HET- have been widely studied, yet at the plot-scale, aquifers in the highly heterogeneous Yeso For- EROGENEITY IN THE YESO FORMATION thinning effects on runoff, soil water flux, and mation. Ground water is recharged in the high ON THE REGIONAL HYDROGEOLOGY IN water balance are scarcely reported. The objec- mountains and flows to the east and north. Most THE SACRAMENTO MOUNTAINS, New tives of this study were to identify runoff springs and wells with fairly young, fresh mete- Mexico, K. E. Zeigler, zeiglergeo@gmail. zones and to calculate soil water fluxes prior to oric waters are found in the high mountains area, com, ZGC, Albuquerque, New Mexico 87123; mechanical thinning of mixed conifer stands. whereas wells farther east along the Pecos Slope B. T. Newton, and S. S. Timmons, New Mexico The study was carried out on private property have older, more chemically evolved signatures Bureau of Geology and Mineral Resources, near James Canyon approximately 20 km east due to longer water-rock interactions. These New Mexico Institute of Mining and Technol- of Cloudcroft, New Mexico. The study site is chemical changes in the ground water may also ogy, Socorro, New Mexico 87801 underlain by San Andres Limestone and Yeso Formation and mainly composed of Douglas-fir be affected by lithologic changes within the Yeso During the spring of 2009, four shallow wells and San Andres Formations. (Pseudotsuga menziesii) and ponderosa pine (Pinus with total depths from 80 to 420 ft were drilled ponderosa) with a tree density average of 770 trees on private property along James Canyon, located ha-1. Soil type is Typic Argiborolls-Aquic Hap- approximately 6 mi east of Cloudcroft, in south- THE SACRAMENTO MOUNTAINS WATER- loborolls with loam and clay loam soil textures. eastern New Mexico. Three of these wells were SHED STUDY: PRE-TREATMENT ANALY- Two plots (90 × 90 m each) were selected at each drilled as monitoring wells as part of the Sacra- SES AND CONSIDERATIONS, B. T. Newton, of four locations characterized by combinations mento Mountains watershed study being done [email protected], New Mexico Bureau of of site (hilltop, slope bottom) and aspect (north- by the New Mexico Bureau of Geology and Min- Geology and Mineral Resources, New Mexico facing, south-facing). Runoff evaluation prior to eral Resources. All four wells were located with- Institute of Mining and Technology, Socorro, mechanical treatment was carried out in late June in 2.5 mi of each other. Water level elevations in New Mexico 87801; A. Fernald, and H. Garduño, and early July in 2009. A total of 24 rainfall simula- the monitoring wells range from 7,102 to 7,916 ft Animal and Range Sciences Department, New tions (three simulations per plot) were done with above sea level, with the shallowest depths to Mexico State University, Las Cruces, New Mex- soil at field capacity. Sixty-min simulated rainfall water at higher elevations and deeper water at 2 ico 88003; and T. Kludt, New Mexico Bureau of was applied to each 1m plot to determine runoff lower elevations. During drilling, well cuttings Geology and Mineral Resources, New Mexico and sediment yield. Infiltration was determined were collected at 10-ft intervals and stratigraphic Institute of Mining and Technology, Socorro, as the difference between simulated rainfall and columns at each well site constructed, in order New Mexico 87801 runoff. A set of three soil moisture and heat dis- to attempt local correlations between wells. This sipation sensors was installed on each plot at There is widespread interest in removing trees to well series demonstrates the regional and local 0.07, 0.20, and 0.35 m depth. Soil water flux was increase water yields in southern New Mexico. heterogeneity of the Yeso Formation, both lat- calculated by Darcy’s equation. Total potential The Sacramento Mountains watershed study erally and vertically. No direct bed-to-bed cor- head was calculated from gravitational and the focuses on: (1) characterization of water bud- relations could be made among any of the four matric potential measured from heat dissipation gets of a mixed conifer forested watershed in the wells. In fact, the four wells do not exhibit the sensors using Retention Curve (RETC) software. southern Sacramento Mountains, New Mexico; same lithology, even where they overlap one The gradient-causing flow was calculated from (2) assessment of the effects of tree thinning on another, despite their relative geographic prox- the sum of gravitational potential and matric the watershed hydrologic system; and (3) evalua- imity. However, tentative correlations between potential from sensors previously mentioned. tion of total watershed surface and ground water the wells and a deep well drilled in Cloudcroft Results showed that runoff and sediment yield outflows. Pre-treatment analyses have been used in 2006 l can be made using transgressive/ were negligible likely due to high infiltration rate to develop a conceptual model of the hydrogeo- regressive cycles identified in the stratigraphic and limestone bedrock. Runoff as a percentage of logic system within the study area and to identify columns. These tentative correlations suggest at total water input was 0.004% at the hilltop and inputs and outputs to the local water budget. least six transgressive events occurred in south- 0.02% at the slope bottom. At the hilltop water Taking place within the bounds of a broader eastern New Mexico during the Permian. flux was 9.34 e-04–2.15 e-04 m h-1, and at the slope regional study, this project addresses two spatial The extreme lateral heterogeneity observed in bottom water flux was 6.64 e-04–2.21 e-04 m h-1. scales: the 750 acre Three L Canyon watershed and the Yeso Formation is apparently a result of local Overall water flux was higher at 7 cm (4.28 e-04 90 × 90 m study plots. The watershed is located on sea level changes during the time of deposition, in m h-1) and 20 cm depth (4.21 e-04 m h-1) than at private property near James Canyon approximate- addition to dissolution collapse due to hydration 35 cm depth (5.21 e-04 m h-1). Regardless of site ly 20 km east of Cloudcroft. There are two springs and dehydration of salts and formation of karst and aspect, infiltration responded rapidly to in Three L Canyon, but no perennial streams that features in the upper Yeso Formation. The effects simulated rainfall where possibilities of deep per- transport water outside the watershed. Elevations of this lithologic heterogeneity combined with colation are greater due to fractured limestone. within the study area range from 2,300 to 2,600 m regional fracture systems on the local and regional Though preliminary results, this study helped to above sea level. Tree densities in the study area hydrogeology is apparent by the high variability improve our understanding of the shallow root average 312 trees/acre, with Douglas fir being the of water level elevations observed in three of the zone water interactions in forested stands. Data

62 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 collected from this study will help to determine are present in most New Mexico and southeast sequence, up to 110 m thick, of rhyolitic fall, flow, thinning effects at plot scale on soil water flux, Arizona diabase, but they are uncommon in and surge deposits interlayered with volcanic runoff, and water balance. northwest Arizona diabase. Feldspar composi- sediments was emplaced beneath the northwest- tions for the Burro and Sierra Ancha Mountains ern volcano flank. The early phase culminated range from An .321 to An 70.43. Pyroxene com- with widespread eruption of coarse-grained, session 4—paleontology positions of the Burro and Sierra Ancha Moun- plagioclase-phyric, trachybasalt to basaltic tra- tains reflect the presence of both clinopyroxene chyandesite flows (2.86–2.76 Ma, n = 3). The final VERTEBRATE ICHNOLOGY OF THE UPPER (augite) and orthopyroxene (hypersthene), and phase (2.8–2.5 Ma) produced intermingled tra- TRIASSIC (APACHEAN) REDONDA FOR- pigeonite. Strontium isotope analyses of Burro chyandesite to trachydacite domes, flows, and MATION, EAST-CENTRAL NEW MEXICO, Mountains diabase show 87Sr/86Sr ratios rang- minor pyroclastic beds cut by a radial swarm of J. A. Spielmann, and S. G. Lucas, New Mexico ing from 0.700624 to 0.705408 for single plagio- trachydacite dikes. These units are intruded by Museum of Natural History and Science, clase crystals, which spans higher than whole a small composite stock of trachydacite to alkali 1801 Mountain Road NW, Albuquerque, New rock values ranging from 0.702076 to 0.703484, rhyolite. As the final phase developed, volcanic Mexico 87104; H. Klein, Rübezahlstr. 1, D-92318 indicating likely assimilation of the host gran- debris flows accumulated on the volcano flanks. Neumarkt, Germany; and A. J. Lerner, New ite by the dikes. We obtained a U-Pb zircon age More than 60 porphyritic to aphyric trachyba- Mexico Museum of Natural History and Sci- of 1115 ± 13 Ma (2s) using LA-MC-ICP-MS on salt lavas and scoria cone deposits (3.3– < 1.7 Ma) a dike from Salt River Canyon in Arizona. This ence, 1801 Mountain Road NW, Albuquerque, are interlayered with MT eruptions and flank age is older than U-Pb baddeleyite ages of 1087 New Mexico 87104 MT on Horace Mesa, Mesa La Jara, and southern ± 3 Ma and 1069 ± 3 Ma obtained from two dia- The Upper Triassic Redonda Formation, the base sills in California (Heaman and Grotzinger Mesa Chivato. Contemporaneous gabbroic intru- uppermost part of the Chinle Group in east- 1992). This discrepancy suggests there are two sions of similar composition (3.1– < 2.8 Ma) creat- central New Mexico, yields extensive vertebrate different aged dike swarms or there was a long ed San Fidel Dome and other small uplifts. Debris ichnofossil assemblages that were first discov- lived magmatic interval. Dikes with ages closer flows and tuffs deposited on mesas adjacent to ered in the 1930s. As much as 92 m thick, the to 1100 Ma may be related to the Midcontinent MT define a possible hiatus in mafic activity that Redonda Formation in its outcrop belt along the rift (Hammond 1990). occurred 2.7–2.2 Ma. The youngest trachybasalt northwestern edge of the Llano Estacado (Gua- complex (Cerro Pelón) is about 1.5 Ma and sits on dalupe and Quay Counties, New Mexico) can the north shoulder of MT. be divided into five members (ascending order): EVOLUTION OF MOUNT TAYLOR COMPOS- Quay (a replacement name for Red Peak), San ITE VOLCANO, NEW MEXICO, F. Goff, candf@ Jon Creek, Duke Ranch, Wallace Ranch, and swcp.com, Department of Earth and Planetary STRATIGRAPHY AND GEOCHEMISTRY OF Montoya Point (laterally equivalent to the Duke Sciences, University of New Mexico, Albuquer- EARLY PYROCLASTIC ERUPTIONS AT Ranch and Wallace Ranch Members). Redonda que, New Mexico 87131; S. A. Kelley, New Mex- MOUNT TAYLOR VOLCANO, NEW MEX- deposition took place in a palustrine system that ico Bureau of Geology and Mineral Resources, ICO, N. W. Dunbar, [email protected], and S. A. comprised a mosaic of lakes, lake margins, flu- New Mexico Institute of Mining and Technol- Kelley, New Mexico Bureau of Geology and vial channels, floodplains, and stable interfluves. ogy, Socorro, New Mexico 87801; G. R. Osburn, Mineral Resources, New Mexico Institute of Most of the Redonda ichnofossil assemblages Earth and Planetary Sciences, Washington Uni- Mining and Technology, Socorro, New Mexico, are from lake margin facies abundantly pre- versity, St. Louis, Missouri 63130; J. R. Lawrence, 87801; F. Goff, Department of Earth and Plan- served in the San Jon Creek Member. Presumed Lawrence GeoServices Ltd. Co., 2321 Elizabeth etary Sciences, University of New Mexico, Street NE, Albuquerque, New Mexico 87112; C. J. lungfish burrows from the Redonda Formation Albuquerque, New Mexico 87131; W. C. McIn- Goff, Geologic Consultant, 5515 Quemazon, Los pertain to Redondarefugium abercrombieorum and tosh, and L. L. Heizler, New Mexico Bureau of Alamos, New Mexico 87544; C. Ferguson, Profes- are vertical to obliquely oriented, slightly heli- Geology and Mineral Resources, New Mexico sional Geologist, 119 North Fork Road, Centen- cal, unlined burrows with a round cross section, Institute of Mining and Technology, Socorro, nial, Wyoming 82055; W. C. McIntosh, New Mex- little ornamentation of the burrow walls, and a New Mexico 87801 flask-shaped terminus. Redonda Formation tet- ico Bureau of Geology and Mineral Resources, rapod footprints are assigned to: Brachychirothe- New Mexico Institute of Mining and Technology, Rhyolitic to trachyandesitic pyroclastic deposits rium parvum, Brasilichnium elusivum, Characichnos Socorro, New Mexico 87801; K. Fellah, School of exposed in three canyons (La Mosca, San Mateo, ichnosp., Evazoum ichnosp., Grallator cursorius, Earth and Environmental Sciences, Washington and Water) around the Mount Taylor edifice pro- Gwyneddichnium (= “Apachepus”) cottonorum, State University, Pullman, Washington 99164; vide insight into early eruption processes at this and Rhynchosauroides ichnosp. Redonda tetrapod N. W. Dunbar, New Mexico Bureau of Geology composite volcano. Measured sections coupled footprints represent the Brontopodus ichnofacies, and Mineral Resources, New Mexico Institute of with geochemical analysis of glass allow cor- more specifically the Evazoum ichnocoenosis. Mining and Technology, Socorro, New Mexico relations between the canyon sections and, for The track assemblages of the Chinle represent a 87801; and J. A. Wolff, School of Earth and Envi- some deposits, sourced areas to be determined. A global Late Triassic footprint record dominated ronmental Sciences, Washington State Univer- 4-m-thick pyroclastic surge and ash-fall deposit by the tracks of crurotarsans, dinosaurs, and sity, Pullman, Washington 99164 at the base of the La Mosca Canyon section, dated at 3.26 ± 0.04 Ma, correlates chemically and sphenodonts. Detailed mapping of four 1:24,000 quadrangles chronologically with 3.3 Ma Grants Ridge high augmented with > 40 40Ar/39Ar dates, > 100 silica rhyolitic deposits sourced 15 km south- major and trace element analyses, and previ- west of Mount Taylor. Overlying this deposit is a session 5—magmatism and volcanism ously published data provide new insights on 1-m-thick rhyolitic pyroclastic surge. Both depos- MESOPROTEROZOIC DIABASE IN SOUTH- the evolution of Plio–Pleistocene Mount Taylor its are absent in the nearby San Mateo Canyon, WESTERN NORTH AMERICA: A PRO- (MT) composite volcano. MT is one of a string where instead, a > 28-m-thick, complex sequence POSAL FOR REGIONAL MAGMATISM, of Miocene–Quaternary volcanoes erupted of rhyolite ignimbrites and pyroclastic surges is R. M. Bright, [email protected], and J. M. along the northeast-trending Jemez lineament found at the base of the exposed stratigraphic Amato, Department of Geological Sciences, and overlies Jurassic–Cretaceous sedimentary section. An ignimbrite in Water Canyon is chemi- 3 New Mexico State University, Las Cruces, New rocks of the Colorado Plateau. The 20-km edi- cally similar to the upper part of the basal San Mexico 88003 fice is constructed of mildly alkaline volcanic Mateo pyroclastic sequence. Above these pyro- rocks of basanite to alkali rhyolite composition. Timing and petrogenesis of a Mesoproterozoic clastic surge and flow deposits in San Mateo mafic dike swarm in southwestern North Amer- Most mafic rocks contain phenocrysts of olivine Canyon, a series of small, chemically correlated, ica is poorly understood. Existing diabase ages and plagioclase, whereas intermediate to silicic pyroclastic fall deposits are found in San Mateo range from 1200 to 1080 Ma, but most have poor rocks contain phenocrysts of plagioclase, horn- and La Mosca Canyons. Two rhyolitic ash falls precision. Diabase samples collected from the blende and/or biotite. Rare trachybasalts contain (one dated to 3.08 ± 0.2 Ma), and a thin, dark- Organ and Burro Mountains of southern New phlogopite. Trachydacites and rhyolites may colored trachyandesite fall deposit are present. Mexico and from the Salt River Canyon, Sierra contain alkali feldspar and quartz. Virtually all The upper of the two rhyolitic ash falls is also Ancha, Pinaleno, Santa Catalina, Hualapai, and volcanics contain clinopyroxene. found in Water Canyon. Above this sequence Garnet Mountains of eastern and northwest- Volcanism began with eruption of basanite of ash falls, a thick (~ 22 m) rhyolitic pyroclastic ern Arizona intrude Proterozoic sediments and lavas (3.6 Ma) and a distinctive fine-grained tra- flow sequence is present in San Mateo Canyon granites in the form of dikes and sills. Diabases chyte (3.3 Ma) followed by multiple eruptions that chemically correlates with a thin (< 1 m) are typically medium grained with ophitic and of alkali rhyolite to trachyandesite lavas, domes, pyroclastic fall in La Mosca Canyon. All these subophitic texture and have plagioclase laths, and pyroclastic deposits (3.1–2.8 Ma). Dur- pyroclastic beds are probably sourced from sites near ~ 1 mm in length. Subhedral olivine crystals ing the first period, a heretofore unrecognized within Mount Taylor.

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 63 The chemical trend of the pyroclastic sequenc- exposure during sea-level fall/lowstand. These their type sections, Myers members of the “Wild es in the canyons ranges from high silica to low asymmetric facies patterns suggest abrupt trans- Cow Formation” clearly are fusulinid-based, bio- silica rhyolite, consistent with derivation from a gression above the underlying cycle cap fol- stratigraphic units, not lithostratigraphic units, as single, normally zoned magma chamber. How- lowed by gradual regression through most of their contacts are not drawn at laterally traceable ever, the presence of the trachyandesitic tephra cycle development. lithologic changes. Thus, Sol se Mete Member = layer in the middle of the sequence may argue δ18O trends for three of the four sampled cycles Missourian fusulinids (= Bartolo–lower Tinajas), instead for multiple, small magma batches. Indi- record 0.8‰ to 1.2‰ up-cycle increases, which is Pine Shadow Member = early Virgilian fusulin- vidual pyroclastic flow/surge deposits appear to consistent with a glacio-eustatic origin for cycle ids (= upper Tinajas–lower Burrego), and La Casa have restricted ranges, consistent with small vol- formation. εεNd trends from six of the seven sam- = middle-late Virgilian fusulinids (= upper Bur- ume, high aspect ratio events, possibly related pled cycles are characterized by mid-cycle mini- rego–Moya). We thus recommend abandonment to dome collapse in early Mount Taylor. In con- mum εεNd values (before maximum regression). of all Myers Pennsylvanian lithostratigraphic trast, pyroclastic fall deposits, although small, We interpret that maximum influx of local fluvial terms because they are either synonyms of earlier are more widespread, and are deposited in all sediment (lowest εεNd values) occurred during named units or do not identify useful lithostrati- three canyons, allowing correlation between the interglacial intervals when the local paleotropi- graphic units. stratigraphic sections. cal climate was wettest, and minimum fluvial influx (maximum εεNd values) occurred during glacial intervals when the climate was the driest. 40 39 session 6—Climate Ar/ Ar GEOCHRONOLOGY, MAGNETIC- This interpretation is supported by Pleistocene POLARITY STRATIGRAPHY, AND TEPH- climate records, which show that during glacial ROCHRONOLOGY OF PLIO–PLEISTO- THE INFLUENCE OF ANTECEDENT SNOW- intervals, the tropics were drier, whereas dur- PACK, AEROSOLS AND ENSO ON THE CENE DEPOSITS IN THE ALBUQUERQUE ing interglacial intervals, the tropics were wet- BASIN, RIO GRANDE RIFT, NEW MEXICO, NORTH AMERICAN MONSOON, J. Sturgis, ter. These preliminary results suggest that local and D. S. Gutzler, Department of Earth and S. D. Connell, [email protected], New Mex- paleotropical climate changes and associated ico Bureau of Geology and Mineral Resourc- Planetary Sciences, University of New Mexico, continental weathering were influenced by the Albuquerque, New Mexico 87131 4 5 es–Albuquerque Office, New Mexico Institute same 10 –10 yr mechanisms that drove Middle of Mining and Technology, Albuquerque, New The factors influencing the North American Pennsylvanian glacio-eustasy. Mexico 87106; G. A. Smith, and J. W. Geissman, monsoon and New Mexico’s summer precipi- Department of Earth and Planetary Sciences, tation are investigated using statistical relation- University of New Mexico, Albuquerque, New ships. Antecedent conditions, including snow- session 7—Stratigraphy Mexico 87131; W. C. McIntosh, N. W. Dunbar, D. pack, spring wildfires and other aerosol forcing, W. Love, and S. M. Cather, New Mexico Bureau and sea surface temperature (SST) in the Niño REVISED PENNSYLVANIAN LITHOSTRAT- of Geology and Mineral Resources, New Mexi- 3.4 region of the equatorial Pacific, have each IGRAPHY IN THE MANZANO MOUN- co Institute of Mining and Technology, Socorro, been linked to the onset of the monsoon or the TAINS, NEW MEXICO, S. G. Lucas, spencer. New Mexico 87801 total precipitation during the monsoon season. [email protected], New Mexico Museum of Natural History and Science, 1801 Mountain This study aims to synthesize several previous The geochronology of alluvial deposits in the Road NW, Albuquerque, New Mexico 87104; studies by considering all of these antecedent Albuquerque Basin are refined using 20 previously and K. Krainer, Institute of Geology and Paleon- variables, in order to produce a multivariate published and 58 new (single-crystal laser-fusion tology, Innsbruck University, Innrain 52, Inns- empirical predictive scheme. and incremental heating) 40Ar/39Ar age deter- bruck, A-6020 Austria High antecedent snowpack and wildfire/aerosol minations and tephrochronologic correlations of forcing are negatively correlated with onset and The Pennsylvanian section at Priest Canyon (primary and reworked) tephra and lavas young- precipitation, whereas the correlation between SST (sec. 7 T3N R5E, Valencia County) includes the er than 10 Ma. These data provide a robust geo- and the monsoon is more complex. These variables type sections of units named by Myers (USGS chronologic framework that was used to develop show different relationships with the monsoon in Bulletin 1372-F) and long applied to Pennsylva- a reversal magnetic-polarity stratigraphy for Plio– two periods, 1961–1990 and 1991–2006; the causes nian strata throughout the Manzano and Man- Pleistocene fluviatile sandstone, conglomerate, of this shift are under investigation. zanita Mountains. Detailed restudy indicates it and mudstone of the Ceja and Sierra Ladrones is very similar to the Pennsylvanian section in Formations (upper Santa Fe Group). Tilt-corrected the Cerros de Amado, ~ 60 km to the southwest, means of all class I (highest quality) sites (normal INSIGHTS INTO THE RELATIONSHIP so, stratigraphic nomenclature introduced by polarity: D = 2.8º, I = 45.0º, n = 58; reverse polarity: BETWEEN CONTINENTAL WEATHERING Thompson in 1942 can be applied at Priest Can- D = 180.2º, I = -41.7º, n = 50) document nearly all AND HIGH-FREQUENCY (104–105 YR) GLA- yon. The base of this section is the ~ 70-m-thick polarity changes (longer than 20 ka) since 4.0 Ma CIO-EUSTASY FROM CYCLOSTRATIGRA- Sandia Formation, mostly covered slopes and and are suitable for correlation to the global polar- 18 beds of sandstone, limestone, and conglomerate ity timescale. The Ceja Formation onlapped the PHY, δ O, AND TRENDS IN εεND, B. Theiling, M. Elrick, Y. Asmerom, and V. Polyak, Department that rest on Proterozoic basement. The overlying late Miocene (ca. 6.3 Ma) Rincones paleosurface, of Earth and Planetary Sciences, University of Gray Mesa Formation (= Los Moyos Limestone) and buried it by about 3.0 Ma. After 3.0–2.6 Ma, New Mexico, Albuquerque, New Mexico 87131 is ~ 190 m thick and mostly cherty limestone, the Ceja Formation became considerably coarser divided into three members (ascending): (1) Ele- grained and carried scattered small boulders. Nd-isotope trends (reported as εεNd) from mod- phant Butte Member, ~ 24 m of limestone and Ceja deposition ended shortly after the Olduvai ern and ancient marine deposits have been uti- shale; (2) Whiskey Canyon Member, ~ 86 m of subchron (1.778 Ma) with the formation of a relict lized to document patterns and changes in marine cherty limestone; and (3) Garcia Member, ~ 83 m depositional surface (Llano de Albuquerque sur- circulation and continental weathering. When of non-cherty limestone and shale with lesser face). Axial-fluvial deposits of the Sierra Ladrones combined with δδ18O trends from marine depos- amounts of cherty limestone, sandstone, and con- Formation (ancestral Rio Grande) had entered the its, we hypothesize that εεNd will provide new glomerate. The overlying Atrasado Formation (= northern part of the basin by late Miocene time insights into local climate fluctuations during Wild Cow Formation) is ~ 272 m thick and divid- (ca. 7 Ma), and through-going axial-river drain- high-frequency (104–105 yr) glacial-interglacial ed into eight members (ascending): (1) Bartolo age was established into southern New Mexico cycles. Here we present whole-rock εεNd, cono- Member, ~ 66 m of slope-forming shale with thin by early Pliocene time (ca. 4.8 Ma). The axial river dont apatite δδ18O, and cyclostratigraphy from beds of sandstone, limestone, and conglomer- once flowed 1–5 km west of the eastern basin- the Middle Pennsylvanian Gray Mesa Formation ate; (2) Amado Member, ~ 8 m of bedded, cherty, bounding fault system before migrating to the of central New Mexico to evaluate potential rela- brachiopod-rich limestone; (3) Tinajas Member, present position of the Rio Grande valley after tionships between glacio-eustasy and continen- ~ 125 m of shale with interbedded limestone and 1.8–1.6 Ma. Deposition of the Sierra Ladrones tal weathering rates during an icehouse climate. sandstone; (4) Council Springs Member, ~ 22 m Formation ceased shortly after the beginning of Samples were collected from seven consecutive of mostly algal limestone without chert; (5) Bur- the Brunhes polarity chron (0.781 Ma), and before high-frequency cycles (2–4 m thick). Upward- rego Member, ~ 18 m of arkosic red beds and deposition of the oldest known inset fluvial ter- shallowing facies trends within the cycles are limestone; (6) Story Member, ~ 7 m of limestone; race deposit in the Rio Grande valley near Albu- characterized by thin-bedded skeletal mud- (7) Del Cuerto Member, ~ 15 m of arkosic red querque, which contains the 0.64 Ma Lava Creek stone/wackestone (deep subtidal facies), over- beds and limestone; and (8) Moya Member, B ash. Valley incision abandoned an early Pleis- lain by massive skeletal wackestone/packstone ~ 11 m of bedded limestone and shale. At the top tocene basin floor and flanking piedmont slopes (shallow subtidal facies), and are commonly of the Pennsylvanian section, the Bursum Forma- of the Sunport, Las Huertas, and Llano de Man- capped by calcretes, regolith breccias, and/or tion is at least 30 m of interbedded red-bed mud- zano surfaces. Incision of the Rio Grande in cen- δδ13C values indicative of prolonged subaerial stone, sandstone, conglomerate, and limestone. At tral and southern New Mexico began before the

64 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 0.45 Ma age of breaching of Lake Alamosa (San An inventory of 29 springs on the Zuni Reserva- Plant debris, including partial walchian fronds Luis Basin) in the headwaters region of Colorado tion conducted between 2007 and 2009 focused and cordaitalean material, and poorly preserved and may not be a direct result of drainage capture on four areas: Nutria, Pescado, Dowa Yalanne- conchostricans are common in the clam-bearing in the upper Rio Grande. Black Rock, and Ojo Caliente (northeast, east- stratum. central, central, and southwest regions of the The clams are equivalved, inequilateral, and reservation, respectively). Springs discharge elongate oval in shape. The hinges are straight session 8—hydrology from the Permian San Andres–Glorieta (Psg), and adductor muscle scars are absent or not pre- Triassic Chinle, Triassic–Jurassic Wingate–Zuni, served. Length ranges from ~ 8 to 26 mm. The TRANSFERABILITY OF PARAMETERS FOR and interconnected Quaternary alluvium/frac- beaks are anteriorly inclined, and the umbones HYDROLOGIC MODELING OF UNGAGED tured basalt (Qal/Qb) aquifers. Spring assess- WATERSHEDS USING THE SOIL AND are slightly inflated and located at ~ 0.25 of length ments included geologic mapping, measurement from the anterior end. Ornamentation consists WATER ASSESSMENT TOOL, A. El-Sadek, of discharge and field water quality parameters, only of concentric growth ridges. Two variants, Department of Plant and Environmental Scienc- spring classification, and geochemical analyses. es, New Mexico State University, Las Cruces, Relatively high-volume springs (100–300 gpm) one with a rounded posterior end, and the other New Mexico 88003; M. Bleisweiss, Department discharge from the Psg and Qal/Qb aquifers. more blunt, may represent sexual dimorphs. of Entomology, Plant Pathology, and Weed Sci- Psg springs in the Nutria area, near the recharge Average height-to-length ratio (= 0.35), allomet- ence, New Mexico State University, Las Cruces, source in the Zuni Mountains, exhibit a mixture ric growth constant, and overall morphology New Mexico 88003; M. Shukla, Department of of modern (< 5–10 yr old) and pre-1952 recharge, including the two variants are very similar to Plant and Environmental Sciences, New Mex- indicating spring discharge from shallow and the Permian anthracosiid, Palaeanodonta, recently ico State University, Las Cruces, New Mexico deep circulation systems near the mountain reported from the El Cobre Canyon Formation of 88003; A. Fernald, Department of Animal and front. Ojo Caliente Psg springs are fenn-type the Cutler Group in the Chama Basin. The Cut- Range Sciences, New Mexico State University, springs that represent predominantly or entire- ler Group record is Wolfcampian and in a differ- Las Cruces, New Mexico 88003; and S. Guldan, ly pre-1952 recharge. Stable isotope (δδ18O and ent Paleozoic basin from the Rowe–Mora Basin Department of Plant and Environmental Sci- δδ2H) data are consistent with high elevation, record, implying possible riverine connections ences, Sustainable Agriculture Science Center winter precipitation recharge for Nutria area Psg between the two basins. at Alcalde, P. O. Box 159, 371 County Road 40, springs and a lower elevation North Plains/Con- Alcalde, New Mexico 87511 tinental Divide recharge source southeast of the reservation for the Ojo Caliente springs. Alluvial A common problem in applied hydrology is the EARLY PERMIAN VERTEBRATE FOSSILS springs in the Black Rock area exhibit modern estimation of hydrological behavior of ungaged FROM THE ABO FORMATION AT THE recharge, whereas discharge from Pescado area watersheds. One approach to this problem is to ABO MINE, ABO PASS, NEW MEXICO, K. alluvial springs represents predominantly pre- use comparative hydrology, which seeks to trans- L. McKeighen, Jr., [email protected], and 1952 recharge. These data indicate that Pescado fer hydrological information from a gaged site to H. W. McKeighen, 46 Cuerro Lane, Los Lunas, area springs discharge from a deeper (possibly the ungaged site. The main objective of this study New Mexico 87031, S. G. Lucas, J. A. Spielmann, leaky-confined) alluvial/fractured basalt flow is to implement this strategy on watersheds in and S. K. Harris, New Mexico Museum of Nat- system, whereas Black Rock alluvial springs dis- New Mexico using model calibration and vali- ural History and Science, 1801 Mountain Road charge from a shallow, unconfined alluvial flow dation to solve the problem of the lack of stream NW, Albuquerque, New Mexico 87104 system. Springs discharging from the Chinle and flow records. This is being accomplished using Zuni/Wingate aquifers exhibit variable recharge, The Abo mine (Scholle mine) is a red-bed copper the physically based, distributed Soil and Water with some receiving rapid recharge from winter deposit developed in the Scholle Member of the Assessment Tool (SWAT). Our approach is to precipitation and others showing older recharge Lower Permian Abo Formation near Abo Pass use gaged watersheds as surrogates for ungaged from summer monsoons. watersheds so that our results can be verified. in Torrance County, New Mexico. It was first Spring discharge measurements conducted The two ways in which hydrologic information worked from 1914 to 1919 and again during the during this investigation, when compared to ear- can be transferred within or between watersheds mid-1940s for both WWI and WWII war efforts. lier studies conducted by Orr (1987) and Sum- are via a spatial or a temporal transformation. Total production of copper, for both periods of mers (1972), suggest a generally declining trend We have accomplished the temporal transfor- operation, was approximately $250,000. The in spring flows between 1972 and 2009. This mation of parameters in the Mimbres Basin of difficulty and cost associated with extracting apparent trend is supported by Zuni research, southwest New Mexico during the period from the copper caused a discontinuation of mining which identified several historically productive, 2002 to 2008 using several different scenarios: efforts after WWII. However, the mine is an although low-discharge, springs that were dry transfer parameters from the period 2002–2005 important fossil locality. Thus, Charles B. Read during 2007–2009 site visits. to 2005–2008, from 2005–2008 to 2002–2005, of the U.S. Geological Survey collected petrified and from 2003–2006 to 2005–2008. These three wood and Calamites specimens from the mine scenarios resulted in Nash-Sutcliffe Efficiencies area in the mid-1940s. One of us (KLM) visited (NSE) of 0.40, 0.44, and 0.43, respectively. The Poster session 1—paleontology the mine in April 2009 and collected the first spatial transfer within a watershed has already and stratigraphy vertebrate fossil from the area, a partial meta- been conducted, i.e., a NSE was 0.64 when tarsal. Additional field work identified highly transferring parameters from Embudo Creek to A POPULATION OF NONMARINE BIVALVES fossiliferous sites at the Abo mine, including Rio Pueblo near Peñasco and it was -0.22 when (UNIONOIDA: ANTHRACOSIIDAE) FROM a stream channel lag associated with an open parameters were transferred from Rio Pueblo THE LOWER PERMIAN (WOLFCAMPIAN) pit mine. This lag consists of both consolidated near Peñasco to Embudo Creek (Embudo Creek SANGRE DE CRISTO FORMATION IN THE sandstone, containing up to 50% or more bone, contains the Rio Pueblo in its upper reaches). ROWE–MORA BASIN, NORTH-CENTRAL and an unconsolidated mudstone, with loose In addition to the temporal and within water- NEW MEXICO, L. F. Rinehart, and S. G. Lucas, bone. The vertebrate fossils from the mine are shed transformation of parameters, we are also New Mexico Museum of Natural History and dominated by bones of the pelycosaur-grade performing a spatial transformation among five Science, 1801 Mountain Road NW, Albuquer- synapsid Sphenacodon. The most diagnostic ele- watersheds in northern New Mexico: Vermejo que, New Mexico 87104 ments are vertebrae with tall, blade-like neural River near Dawson, Cimarron River near Cimar- spines. The presence of Sphenacodon within the ron, Rio de Taos below Los Cordovas, Embudo We describe a rich deposit of thin-shelled, fresh- Creek at Dixon, and the Jemez River near Jemez. water bivalves that constitute the first docu- assemblage indicates an Early Permian (Coyo- The details of this work and the results of the mented occurrence of these clams in the Penn- tean–Seymoran: Wolfcampian) age. spatial transformation will be discussed. sylvanian–Permian Sangre de Cristo Formation of the Rowe–Mora Basin. The clams are from laminar, greenish-gray, micaceous shale beds of DIMETRODON (EUPELYCOSAURIA: SPHEN- INVENTORY OF SPRINGS ON ZUNI TRIBAL lacustrine origin at NMMNH locality 7889 near ACODONTIDAE) FROM THE UPPER LANDS IN WEST-CENTRAL NEW MEXICO: Glorieta Pass (T15N R11E, Santa Fe County) in PERMIAN ABO FORMATION, TORRANCE IMPLICATIONS FOR AQUIFER RECHARGE the upper part of the Sangre de Cristo Forma- COUNTY, NEW MEXICO, H. W. McKeighen, IN THE ZUNI MOUNTAINS AND NORTH tion. These strata are of probable Early Permian [email protected], and K. L. McKeighen, PLAINS, P. Drakos, [email protected], (Wolfcampian) age. The clams are preserved as Jr., 46 Cuerro Lane Los Lunas, New Mexico and J. Riesterer, Glorieta Geoscience, Inc., P. O. external and (rarely) internal casts that typically 87031; S. G. Lucas, J. A. Spielmann, and S. K. Box 5727, Santa Fe, New Mexico 87501; and K. lie on the bedding planes with the articulated Harris, New Mexico Museum of Natural His- Bemis, Zuni Conservation Program, P. O. Box valves closed, although some show the paired tory and Science, 1801 Mountain Road NW, 339, Zuni, New Mexico 87327 valves wide open (~ 180°) and the hinge intact. Albuquerque, New Mexico 87104

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 65 The sail-backed basal (“pelycosaurian”-grade) mapping (especially USGS Map I-968), which THE BURROW ZOOPHYCOS IN PENNSYL- synapsid Dimetrodon is one of the most distinc- located the Kinney quarry stratigraphically high VANIAN STRATA OF THE MUD SPRINGS tive basal amniotes of the Permian Period. Out- in Myers’ (1973, USGS Bulletin 1372-F) “Pine MOUNTAINS, SIERRA COUNTY, NEW side of Texas, the genus has sparse records in Shadow Member” of the Wild Cow Formation, MEXICO, S. G. Lucas, spencer.lucas@state. New Mexico, Utah, Arizona, and Germany. We a local map unit that fusulinid biostratigraphy nm.us, New Mexico Museum of Natural His- add to the sparse record of Dimetrodon from New (in other parts of the mountain range) indicates tory and Science, 1801 Mountain Road NW, Mexico a recently discovered specimen from the is of middle Virgilian age. In contrast, we have Albuquerque, New Mexico 87104; K. Krainer, Abo Pass area, Torrance County, consisting of developed three datasets that indicate the Kin- Institute of Geology and Paleontology, Inns- a distinctive elongate neural spine cataloged as ney quarry is older—stratigraphic position, bruck University, Innrain 52, Innsbruck, A-6020 NMMNH P-58748. From the lower part of the fusulinids, and conodonts. Our detailed local Austria; J. A. Spielmann, and A. J. Lerner, New Cañon de Espinoso Member of the Abo For- lithostratigraphic studies coupled with regional Mexico Museum of Natural History and Sci- mation near the Abo mine (NMMNH locality stratigraphic investigations indicate the Kinney ence, 1801 Mountain Road NW, Albuquerque, 7765), the incomplete spine has a figure-eight quarry is in the Tinajas Member of the Atrasado New Mexico 87104 (or dumbbell-shaped) cross sectional outline, a Formation, so it is stratigraphically lower (i.e., Zoophycos comprises a diverse group of spreite minimum dorsoventral height of 125 mm and a very near the base of Myers’ “Pine Shadow burrows that range in age from Ordovician to maximum transverse width of 12 mm. Slender, Member”) than suggested by previously pub- Recent. It is generally thought to be the feed- elongate neural spines with anterior and poste- lished maps. A laterally extensive fusulinid-bear- ing trace of various worm-like animals and to rior grooves (forming a figure-eight cross sec- ing limestone a few meters below the level of the indicate poorly oxygenated paleoenvironments tion) are particularly characteristic of the genus. Kinney quarry yields an early-middle Missou- with low sedimentation rates. There are only a However, NMMNH P-58748 is too incomplete to rian fusulinid assemblage consisting of Tumu- few published reports of Zoophycos from New assign to a species of Dimetrodon, though it clear- lotriticites cf. T. tumidus and species of Triticites: Mexico, and these are primarily from Carbon- ly pertains to a small specimen of the genus. T. cf. T. planus, T. cf. T. myersi, and T. ex gr. T. ohio- iferous strata. We add to this sparse record an This fossil of Dimetrodon is the fourth record of ensis. Conodonts from the basal beds of the Kin- occurrence of Zoophycos at Whiskey Canyon in the genus from New Mexico. Two are from Abo the Mud Springs Mountains. Here, the Zoophycos Formation red beds in the Jemez Mountains area ney quarry are also Missourian species, though they indicate an age slightly younger than do the fossils occur in a 0.6-m-thick bed of coarse cri- of northern New Mexico and a third is from the noidal limestone (crinoidal wackestone) near the Loma de las Cañas area, Socorro County. During fusulinids. Thus, the Kinney conodont fauna is dominated by members of the Idiognathodus sym- top of the Elephant Butte Formation of Thomp- the time of Abo deposition (middle Wolfcam- son, which is near the top of the Red House For- metricus—I. multinodosus group, species of which pian–early Leonardian), the Dimetrodon locality mation of Kelley and Silver. appear in the middle Missourian and range into reported here was ~ 170 km from the seashore We collected a representative specimen pre- the Virgilian (middle Kasimovian into the base and near the flanks of the Pedernal uplift of the served in convex hyporelief. It shows clockwise, of the Gzhelian). We conclude that the Kinney ancestral Rocky Mountain orogeny. This Dime- alectorurid (“cock’s tail”) spreite on the bedding trodon thus lived in an inland habitat, and this quarry Lagerstätte is of Missourian age, most surface. Because neither a marginal tube nor a fits the distribution of Dimetrodon fossils in the likely middle Missourian. vertical generating tunnel is preserved, the spec- Abo Formation in New Mexico, which is consis- imen can only be assigned to cf. Zoophycos ich- tent with it having been a fully terrestrial inland nosp. The overall width is approximately 27 cm, and upland predator. Additional discoveries of EXCEPTIONALLY PRESERVED PALEOFLO- which is average size for Paleozoic forms. Zoo- Dimetrodon, like that reported here, are needed to RA FROM THE UPPER TRIASSIC CHINLE phycos is a classic trace fossil long interpreted as fully establish its paleogeographic and paleoen- GROUP, SANTA FE COUNTY, NEW MEX- characteristic of relatively deep, poorly oxygen- vironmental range, though we expect that full ICO, S. G. Lucas, [email protected], ated sea bottoms. However, protected lagoonal explanation of its varied abundance will remain and J. A. Spielmann, New Mexico Museum of settings of moderate depth are also known to elusive for some time to come. Natural History and Science, 1801 Mountain produce Zoophycos, and we interpret the Mud Road NW, Albuquerque, New Mexico 87104 Springs record as a shallow marine setting with restricted circulation. The Zoophycos bed is in PRECISE AGE OF THE KINNEY BRICK A recently discovered locality in the Trujillo the middle of a 20-m-thick succession of wavy QUARRY LAGERSTÄTTE, PENNSYLVA- Formation, Chinle Group, south of Lamy, Santa to even bedded limestone units (0.6–2.8 m thick) NIAN OF THE MANZANITA MOUNTAINS, Fe County, New Mexico (T12N R11E), yields and covered intervals (0.6–2.9 m thick) that prob- NEW MEXICO, S. G. Lucas, spencer.lucas@ a remarkably well-preserved Upper Triassic ably represent shale intervals. These limestone state.nm.us, New Mexico Museum of Natu- paleoflora. The fossil plants come from two units are all dark gray, micritic, and contain some ral History and Science, 1801 Mountain Road stratigraphic levels in an ~ 1-m-thick bed of chert in the lower and upper part. The lime mud- NW, Albuquerque, New Mexico 87104; K. muddy, micaceous fine-grained sandstone and stone in the upper part of the section, above the Krainer, Institute of Geology and Paleontology, siltstone. Locally, the Trujillo Formation is ~ 24 m Zoophycos bed, is bioturbated. Common fossils Innsbruck University, Innsbruck, Austria; B. thick, and the plant levels are ~ 18 m below its are brachiopods and crinoid fragments. The D. Allen, New Mexico Bureau of Geology and contact with the overlying Petrified Forest For- muddy texture of the limestone units indicates Mineral Resources–Albuquerque Office, New mation. We interpret the plant-bearing bed as deposition in a low-energy shelf environment Mexico Institute of Mining and Technology, a shallow lacustrine deposit that developed on below the storm wave base. Albuquerque, New Mexico 87106; J. E. Barrick, the floodplain surface between Trujillo channel Department of Geosciences, Texas Tech Uni- courses. The paleoflora is dominated by carbon- versity, Lubbock, Texas 79409; and D. Vachard, ized compressions of two taxa, the palmate fern ATTEMPTED RELOCATION OF THE 1941 UNIVERSITY OF OKLAHOMA Université des Sciences et Technologies de Lille, Phlebopteris smithii (Daugherty) (including com- PENTACER- ATOPS QUARRY, SAN JUAN COUNTY, NEW Villenueve d’Ascq, France plete, monopodial palmate leaves) and the ben- MEXICO R. K. Hunt-Foster Located in the Manzanita Mountains of cen- nettitalean Otozamites powelli (Fontaine). Much , , rebecca.k.hunt@ gmail.com, Museum of Western Colorado, tral New Mexico, the Kinney Brick quarry is a less common plants include the fern Todites fra- Dinosaur Journey, 550 Jurassic Court, Fruita, world famous Late Pennsylvanian fossil locality gilis Daugherty and the horsetail Neocalamites. Colorado 81521; T. E. Williamson, New Mex- in an estuarine deposit. The quarry is located The quality of preservation of this macroflora is ico Museum of Natural History and Science, in the Atrasado Formation (locally designated exceptional, encompassing epidermis, sporangia, 1801 Mountain Road NW, Albuquerque, New the “Wild Cow Formation” in previous stud- and spores. This paleoflora is characteristic of the Mexico 87104; and N. R. Longrich, Department ies), a regionally extensive stratigraphic unit of Dinophyton floral zone, yet it is stratigraphically of Geology, Yale University, New Haven, Con- well-established Late Pennsylvanian age, based high for an occurrence of this floral zone. Thus, necticut 06520 on fusulinid biostratigraphy. However, the pre- the overlying Sanmiguelia floral zone normally is cise age of the Kinney quarry deposit has been found in Trujillo Formation strata. Nevertheless, In July 1941, J. W. Stovall of the University of difficult to determine because virtually all of near Las Vegas in San Miguel County, Sanmigue- Oklahoma, with graduate student Don Savage the fossils from the quarry are not precise age lia has been found below the Trujillo Formation, and undergraduate Wann Langston, Jr., traveled indicators. Thus, the age assigned to the Kinney in the uppermost Garita Creek Formation. The to the San Juan Basin of New Mexico to collect quarry (middle Virgilian) has long been based Lamy locality thus adds to evidence that there is fossils for the University of Oklahoma Museum. more on its inferred lithostratigraphic position a stratigraphic overlap between the Dinophyton While on this trip they discovered the remains of than on biostratigraphic indicators at the quarry. and the Sanmiguelia floral zones in the middle the largest and most complete specimen of Penta- This age assignment has relied on USGS geologic part of the Chinle Group. ceratops sternbergi (OMNH 10165), a ceratopsian

66 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 dinosaur that is probably endemic to the late CRANIAL ANATOMY AND TAXONOMY OF fossils in the overlying Naashoibito Member Campanian of the San Juan Basin, New Mexico. SPHENACODON FEROX (EUPELYCOSAU- of the Ojo Alamo Formation. We have repeat- This particular specimen is one of the largest cer- RIA: SPHENACODONTIDAE) FROM THE edly sampled this carbonaceous shale bed, most atopsian dinosaurs ever collected (with a recon- LATE PENNSYLVANIAN–EARLY PERMIAN recently in 2009, and it yields only Cretaceous structed skull length of over three meters), and OF NEW MEXICO, J. A. Spielmann, L. F. Rine- palynomorphs. Thus, the presence of Tschudy- the specimen is on permanent display at the Sam hart, and S. G. Lucas, New Mexico Museum of pollis thalmanni and Equisetosporites multipartitus Noble Museum of Natural History in Norman, Natural History and Science, 1801 Mountain at this locality indicates a Late Cretaceous age, Oklahoma (OMNH). The specimen is certainly Road NW, Albuquerque, New Mexico 87104; probably Maastrichtian. In 2009 we also sampled from either the Fruitland or Kirtland Formations D. S. Berman, and A. C. Henrici, Section of this carbonaceous shale bed at the top of the Kirt- and is considered part of the Hunter Wash local Vertebrate Paleontology, Carnegie Museum land Formation at Willow Wash, ~ 6 km to the fauna. Locating the historic 1941 Pentaceratops of Natural History, 4400 Forbes Avenue, Pitts- northwest, and here it also yields a Cretaceous quarry will help to better constrain the geologic burgh, Pennsylvania 15213; and S. K. Harris, palynomorph assemblage. The presence of abun- age of this particular specimen. Unfortunately, New Mexico Museum of Natural History and dant Tschudypollis thalmanni and T. retusus at this the precise location of this important find has Science, 1801 Mountain Road NW, Albuquer- second locality also suggests a Late Cretaceous been lost. Dr. Langston, documented the find que, New Mexico 87104 age for the sample, probably Maastrichtian. to the best of his recollection, but the site has Sphenacodon is a pelycosaurian-grade synapsid, We therefore consider the report of Paleocene not been relocated. Evidence suggests that it is best known from the Lower Permian of Rio Arri- palynomorphs from this bed at Barrel Spring within an area now included in the Fossil Forest ba County, northern New Mexico. Of the two spe- a non-repeatable result, so it is not reliable for Research Natural Area near Coal Creek. Howev- cies (S. ferox and S. ferocior), S. ferox is known from age assignment. Palynostratigraphy provides no er, some have suggested that the quarry may not comparatively little skull material, and the skulls support for assigning a Paleocene age to dino- be in the documented region, but rather north of historically assigned to the taxon are heavily saur fossils in the west-central San Juan Basin, this area, within what is now the Bisti/De-na-zin reconstructed and composed of few actual cranial New Mexico. Wilderness Area. In April 2009, Nick Longrich elements. In contrast, S. ferocior is known from and ReBecca Hunt-Foster attempted to relocate numerous nearly complete skulls that have been the 1941 University of Oklahoma Pentaceratops extensively illustrated and described in the litera- UPPER CRETACEOUS (TURONIAN) AMMO- quarry, following the notes of Wann Langston, ture. Here, we report on a new, nearly complete NITES FROM THE CARLILE AND JUANA Jr. and archival photographs from the OMNH. skull of S. ferox collected from the eastern wall of LOPEZ MEMBERS OF THE MANCOS SHALE, While the location of this historic quarry was not the Cañon del Cobre in a Sphenacodon-dominated EASTERN SIDE OF MESA PRIETA, SAN- certainly located during the course of this par- bonebed (NMMNH locality 5379). Lithologically, DOVAL COUNTY, NEW MEXICO, P. L. Sealey, ticular search, several other previous quarries the quarry is in a finely laminated, dark reddish- and S. G. Lucas, New Mexico Museum of Natural were identified. brown, immature arkosic sandstone with pale, History and Science, 1801 Mountain Road NW, greenish-yellow banding at ~ 10 cm intervals and Albuquerque, New Mexico 87104 is within the upper vertebrate assemblage zone The zones of Collignoniceras woollgari, Priono- of the Cañon del Cobre (Seymouran land verte- cyclus hyatti, Prionocyclus macombi, Prionocyclus brate faunachron). This new skull demonstrates A NEW ASSEMBLAGE OF UPPER CRETA- wyomingensis, and Prionocyclus novimexicanus are CEOUS SELACHIANS: HOSTA TONGUE numerous cranial differences between S. ferox and S. ferocior including: overall skull size; num- present in the Carlile and Juana Lopez Members OF THE POINT LOOKOUT SANDSTONE, of the Mancos Shale on the eastern side of Mesa BERNALILLO COUNTY, NEW MEXICO, ber of premaxillary teeth; number of precanine maxillary teeth; shape of the ventral maxillary Prieta, Sandoval County, New Mexico. Here, the R. Pence, S. G. Lucas, K. Wright, and J. A. Spiel- Greenhorn interval (with abundant Pycnodonte mann, New Mexico Museum of Natural His- margin; shape of the maxillary step; develop- ment of the dorsal lamina of the maxilla; thick- newberryi) is ~ 7 m thick and is overlain by the tory and Science, 1801 Mountain Road NW, ~ 60-m-thick Carlile Member (locally, no Semilla Albuquerque, New Mexico 87104 ness of the orbital process of the frontal; shape of the anteroventral corner of the temporal fenestra; Sandstone is present) capped by the ~ 36-m-thick A new assemblage of Santonian selachians from shape of the squamosal-jugal suture; shape of the Juana Lopez Member. The ammonite fauna from the eastern side of the Rio Puerco was collected parietals; and extent of the dental field on the pal- the Carlile Member includes Collignoniceras in the summer of 2009. This faunal assemblage atal ramus of the pterygoid. S. ferox has a tempo- woollgari, Tragodesmoceras carlilense, Romanic- was found in unconsolidated sand through ral range from the Late Pennsylvanian (late Virgil- eras mexicanum, Herrickiceras costatum, Spathites both surface picking and screening, and is ian: Coyotean lvf) through the Early Permian (late puercoensis, Prionocyclus hyatti, Placenticeras located in the lower Santonian Hosta Tongue, Wolfcampian: Seymouran lvf), whereas S. ferocior pseudoplacenta, and Coilopoceras springeri in two is restricted to the Coyotean lvf, but does span the which is the lowest horizon of the Point Look- assemblage zones, lower (woollgari) and upper Pennsylvanian–Permian boundary. out Sandstone, which is the lowest of the strati- (hyatti) separated by ~ 25 m of section. The graphic units within the Mesaverde Group. ammonite fauna from the Juana Lopez Member The sands were collected in various locations includes Prionocyclus macombi, Coilopoceras colleti, throughout an area of approximately one acre, NEW PALYNOLOGICAL DATA FROM CRE- Placenticeras sp., Coilopoceras inflatum, Prionocy- TACEOUS STRATA IN THE SAN JUAN and then screen-washed using a 1 mm mesh. clus wyomingensis, Scaphites ferronensis, Prionocy- BASIN, NEW MEXICO, DO NOT INDICATE This process yielded in excess of 200 teeth, clus novimexicanus, and Scaphites whitfieldi, from A PALEOCENE AGE FOR DINOSAUR FOS- representing at least four orders. Within these throughout the member. SILS, R. M. Sullivan, Section of Paleontology Collignoniceras woollgari orders, at least 16 genera can be recognized, The Zone also occurs at and Geology, The State Museum of Pennsylva- other places in New Mexico including the lower including three undescribed taxa that are new nia, 300 North Street, Harrisburg, Pennsylvania part of the Tres Hermanos Sandstone Member to the New Mexican selachian record. The teeth 17120; D. R. Braman, Royal Tyrrell Museum and upper part of the Rio Salado Member at picked from the surface show much wear due of Palaeontology, P. O. Box 7500, Drumheller, Carthage and the lower Carlile Member at Galis- to exposure, but the screen-washed teeth show Alberta T0J 0Y0, Canada; S. E. Jasinski, Section of teo Dam. The Prionocyclus hyatti Zone also occurs little evidence of prior transport. Besides teeth, Paleontology and Geology, The State Museum at other places in New Mexico, including the several dermal ossicles of selachians were also of Pennsylvania, 300 North Street, Harrisburg, Carlile Member at Galisteo Dam and the Semi- found, and teleost fossils, both teeth and ver- Pennsylvania 17120; S. G. Lucas, New Mexico lla Sandstone and Carlile Members at La Ven- tebrae, were present in some abundance. This Museum of Natural History and Science, 1801 tana. The Prionocyclus macombi Zone also occurs assemblage is dominated by lamniform species, Mountain Road NW, Albuquerque, New Mex- at many other places in New Mexico, includ- especially those of Scapanorhynchus, Squalicorax, ico 87104 ing the type and reference sections of the Juana and Cretolamna. Rajiformes (Pseudohypolophus) Claims of Paleocene dinosaur fossils in the San Lopez at Galisteo Dam and La Ventana, respec- and Pristiformes (Ischyrhiza) are also fairly com- Juan Basin have been largely based on palyno- tively. The Prionocyclus wyomingensis Zone also mon. Included in this assemblage are several stratigraphy—namely, that in situ Paleocene-age occurs in the Juana Lopez Member at the type shell fragments of soft-shell turtle (Trionychi- palynomorphs are found stratigraphically below and reference sections, in the D-Cross Member dae) and two pieces of very small reptile teeth. in situ dinosaur fossils. One key locality is Barrel at Cebollita Mesa, and in the D-Cross Member A listing of the selachian fauna would include Springs in the west-central San Juan Basin (sec. at D-Cross Mountain. The zone of Prionocyclus three species of Squalicorax, as well as Cretolam- 17 T24N R11W), where a carbonaceous shale bed novimexicanus also occurs at various New Mexico na, Ptychotrygon, Cantioscyllium, Cretoxyrhina, at the top of the De-na-zin Member of the Kirt- locations, especially in the D-Cross and Juana Scapanorhynchus, Hybodontidae, Cretodus, Pty- land Formation supposedly yielded Paleocene- Lopez Members of the Mancos Shale. The C. chodus, and Odontaspis. age palynomorphs below the in situ dinosaur woollgari Zone is of early-middle Turonian age.

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 67 The P. hyatti and P. macombi Zones are of middle of other limb bones, as well as bones of the right the upper Finlay Formation (youngest cycle of the Turonian age, the P. wyomingensis Zone is of late- pes. The completeness of the skeleton contrasts Fredericksburg Group), lower Mancos Formation middle Turonian age, and the P. novimexicanus with most other collections of O. navajovicus, (base of Greenhorn cycle), and six Washita Group Zone is of late Turonian age. which consist of isolated elements. O. navajovicus cycles: WA1 = Del Norte Formation, WA2 = Smel- differs from all other known species of Ophiacodon tertown Formation, WA3 = Muleros Formation, in the retention of the following primitive charac- WA4 = Mesilla Valley Formation, WA 5 = most of NEW MEXICO’S MOST PROLIFIC UPPER ters: ventral ridge of the postaxial presacral centra Mojado Formation, and WA6 = uppermost Mojado CRETACEOUS SHARK ASSEMBLAGE: are flat with well-defined longitudinal borders, and Del Rio and Buda Formations. HOSTA TONGUE OF THE POINT LOOK- adductor ridge of the femur is weakly developed OUT SANDSTONE, BERNALILLO COUN- and positioned mid-ventrally along the shaft, and TY, NEW MEXICO, K. Wright, J. Bourdon, S. G. the neck of the astragalus is almost half of the ADDITIONAL INVERTEBRATE ICHNOTAXA Lucas, and R. Pence, New Mexico Museum of proximodistal length of the element. The unique FROM THE LOWER PERMIAN HUECO Natural History and Science, 1801 Mountain morphology of the ventral surface of the centrum GROUP, ROBLEDO MOUNTAINS, SOUTH- Road NW, Albuquerque, New Mexico 87104 in O. navajovicus is potentially advantageous in CENTRAL NEW MEXICO, A. J. Lerner, S. G. We present a follow-up to a preliminary analysis the identification of isolated thoracic centra when Lucas, and J. P. MacDonald, New Mexico Museum published in 1989 of a selachian fossil assemblage present in combination with the typical ophiaco- of Natural History and Science, 1801 Mountain in the Upper Cretaceous Hosta Tongue of the dontid wing-shaped transverse process, in which Road NW, Albuquerque, New Mexico 87104 Point Lookout Sandstone along the Rio Puerco a web of bone extends from the diapophyses to Recent collecting of the Lower Permian Robledo drainage in Bernalillo County. The Point Look- the parapophysis and the centrum has a wedge- Mountains Formation within the newly estab- out Sandstone is the lowest stratigraphic unit of shaped cross-sectional outline. Therefore, O. nava- lished Prehistoric Trackways National Monument the Mesaverde Group, and the lower Santonian jovicus can be considered of potential use in Late and from its periphery near Las Cruces, New Hosta Tongue is the lowest horizon of the Point Pennsylvanian tetrapod biostratigraphy. As cur- Mexico, has yielded several previously unre- Lookout Sandstone. An extremely prolific lens rently understood, the stratigraphic distribution corded ichnofossils, all of which are unusual. A of selachian teeth and other fossils is located at of O. navajovicus in New Mexico, Utah, and Colo- resting impression has been found on a small slab NMMNH locality 297. The fossiliferous lens is rado indicate that O. navajovicus characterizes the of mudstone that contains associated Paleohelcura approximately 6 cm thick. Approximately 80 kg Cobrean land-vertebrate faunachron. trackways. The morphology of the impression is of in situ material was processed and screened in consistent with an interpretation of having been a sieve stack down to 0.5 mm mesh. This process produced by a scorpion. Neoichnological experi- yielded about 5,000 selachian teeth that repre- CRETACEOUS DEPOSITIONAL ENVIRON- ments have likewise demonstrated that scorpi- sent members of at least six orders, with at least MENTS AND SEQUENCE STRATIGRAPHY ons can produce Paleohelcura. A bilobed ribbon 30 species represented, including several previ- AT CERRO DE CRISTO REY, DOÑA ANA trail preserved in convex hyporelief on a small ously undescribed genera and species and others COUNTY, NEW MEXICO, K. Krainer, Karl. mudstone slab has also been found. Arthropod new to the New Mexican fossil record. The teeth [email protected], Institute of Geology and appendage impressions appear outside of the show little transport wear. Also present in great Paleontology, Innsbruck University, Innrain lateral margins on either side of the lobes, indi- numbers are small calcified selachian centra 52, Innsbruck, A-6020 Austria; S. G. Lucas, J. A. cating that this is a locomotion trail. Although and small to very small teleost teeth and verte- Spielmann, and K. Durney, New Mexico Museum this specimen resembles some relatively common brae. The assemblage is dominated by Scapano- of Natural History and Science, 1801 Mountain ichnogenera, the presence of appendage impres- rhynchus, Pseudohypolophus, and Ptychotrygon. Road NW, Albuquerque, New Mexico 87104 sions external to the margins is distinctive. This trace fossil probably represents a new ichnotaxon. This dominance of small Lamniformes and Cretaceous marine and nonmarine strata of late durophagous species suggests a shallow water Albian–middle Cenomanian age exposed around Lastly, an enigmatic ovoid burrow preserved in environment, and a terrestrial component sug- the Cerro de Cristo Rey uplift in southern Doña convex hyporelief has been found on a mudstone gests a deltaic condition. This terrestrial compo- Ana County, New Mexico, comprise a section slab that contains Monomorphichnus and tetrapod nent includes teeth of crocodylians, hadrosaurs, ~ 350 m thick and are assigned to the (ascending claw drags. It bears some resemblance to insect and dromaeosaurs and bits of wood and plant order) Finlay, Del Norte, Smeltertown, Muleros, breeding chambers, which are more commonly seeds. Also present in the fauna are teeth and Mesilla Valley, Mojado (= “Anapra”), Del Rio, found in Mesozoic or younger strata. There is one scales of gars and shell fragments of softshell Buda, and Mancos (= “Boquillas”) Formations. previous record of a possible insect chamber from turtles (Trionychidae). Some of the other genera Macro- and microfossils from these strata indicate the Robledo Mountains Formation, which differs represented are: Hybodus, Lonchidion, Ptychodus, that the Finlay, Del Norte, Smeltertown, Muleros, in size and appearance from the ovoid burrow. Squatina, Cederstroemia, Cantioscyllium, Chiloscyl- and Mesilla Valley Formations are of late Albian Although ichnofossils from the Robledo Moun- lium, ?Odontaspis, Carcharias, Squalicorax, Creta- age, whereas the Del Rio, Buda, and Boquillas For- tains Formation have been studied for nearly two lamna, Cretoxyrhina, Protolamna, Ischyrhiza, Sclero- mations are of Cenomanian age. The base of the decades, these newly discovered specimens indi- rhynchus, Texatrygon, Rhinobatos, Protoplatyrhina, Cenomanian is most likely at a trangressive surface cate that continued collecting has a high potential and Myledaphus. within the uppermost Mojado Formation. The late for providing new or unusual ichnotaxa. Albian (Manuaniceras powelli ammonite zone) to early Cenomanian (Neophlycticeras hyatti ammonite THE MOST COMPLETE SKELETON OF OPH- zone) sedimentary succession at Cerro de Cristo Poster session 2—Granite and rock piles IACODON NAVAJOVICUS (EUPELYCOSAU- Rey consists of alternating fossiliferous limestone, RIA: OPHIACODONTIDAE), FROM THE shale with limestone and sandstone intercalations, PETROLOGIC CHARACTERISTICS OF GRA- UPPER PENNSYLVANIAN OF CAÑON DEL and sandstone. Muddy limestone types are com- NITIC PHASES WITHIN THE HERMIT’S COBRE, NEW MEXICO, S. K. Harris, S. G. monly wavy to nodular and represent deposits of PEAK BATHOLITH, R. M. Pitrucha, rpitruch@ Lucas, and J. A. Spielmann, New Mexico Museum an open marine shelf environment below wave live.nmhu.edu, and J. Lindline, New Mexico of Natural History and Science, 1801 Mountain base. Intercalated coquina beds rich in mollusc Highlands University, Environmental Geol- Road NW, Albuquerque, New Mexico 87104 shells are interpreted as storm layers. Shale was ogy Program, Natural Resources Management deposited in an open shelf environment below Department, Las Vegas, New Mexico 87701 The most complete postcranial skeleton known of or near wave base during periods of increased the Late Pennsylvanian pelycosaurian-grade syn- siliciclastic influx. Intercalated thin limestone and We report petrographic and geochemical data apsid Ophiacodon navajovicus is from the Upper sandstone beds are suggested to be storm layers. from granitic phase within the Hermit’s Peak Pennsylvanian interval of the El Cobre Canyon The siliciclastic Mojado Formation is a regressive- batholith, a Proterozoic plutonic-metamorphic Formation (Cutler Group) at Cañon del Cobre, transgressive succession formed in depositional complex in the southern Sangre de Cristo Moun- Rio Arriba County, New Mexico. The skeleton was environments ranging from lower shoreface to tains northwest of Las Vegas, New Mexico. We preserved in brownish-red mudstone with blue upper shoreface and even fluvial sediments, again recognize at least three distinct intrusive phases. concretions located approximately 80 m below overlain by shallow marine siliciclastics. Although Early granitoid intrusions formed centimeter- the contact of the El Cobre Canyon Formation the Washita Group section at Cerro de Cristo Rey to meter-wide coarse-grained tabular sheets and the overlying Arroyo del Agua Formation. is much thicker and displays some differences and layers within Paleoproterozoic host rock Cranial elements are represented by fragments in facies, the succession shows similar transgres- gneisses. The intrusions were deformed dur- of the right maxilla and dentary. The postcranial sive and regressive trends when compared to the ing isoclinal folding along with their host rocks, elements include vertebrae representative of all Washita Group of North Texas. Thus, we recognize suggesting that these early granites are pre- or regions of the vertebral column, a nearly com- eight unconformity-bounded depositional cycles syntectonic with contractional deformation asso- plete pelvis, a complete right femur and portions in the Cretaceous section at Cerro de Cristo Rey, ciated with Yavapai–Mazatzal collision. These

68 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 granites show a fine- to medium-grained anhe- Local Polynomial Interpolation did not produce A REGIONAL WATER TABLE MAP AND dral granular texture with quartz microstruc- realistic models. Ultimately, however, the very WATER LEVEL VARIATIONS IN THE tures indicative of dynamic strain and solid state nature of the pyrite and fluoride distribution SOUTHERN SACRAMENTO MOUNTAINS deformation, including undulose extinction, within the rock pile makes any model unreal- WATERSHED, NEW MEXICO, L. Land, lland@ serrated grain boundaries, and ribbon texture. istic. In the 30 yrs since the rock pile’s emplace- gis.nmt.edu, New Mexico Bureau of Geology The Hermit’s Peak granite, a supposed 1.4 Ga ment, not enough weathering had occurred to and Mineral Resources, and the National Cave “anorogenic”granite, is a foliated fine- to medi- preferentially relocate and concentrate pyrite and Karst Research Institute, New Mexico Insti- um-grained anhedral granular granite. Aligned or fluoride. In the rock pile, pyrite and fluoride tute of Mining and Technology, 1400 Commerce interstitial minor biotite and magnetite define are still randomly distributed and dependent Drive, Carlsbad, New Mexico 88220; G. C. Rawl- ing, New Mexico Bureau of Geology and Min- the foliation, which is variable at the outcrop- on where loads of mined rock were dumped, eral Resources–Albuquerque office, New Mex- scale. The relationship between the granite folia- rather than distributed by some physical pro- ico Institute of Mining and Technology, Albu- tion and host rock foliation has not been con- cess that can be effectively modeled. cluded. Strain-related microstructures are rare, querque, New Mexico, 87106; S. S. Timmons, suggesting that the Hermit’s Peak granite fabric New Mexico Bureau of Geology and Mineral developed syntectonically within a local or more poster session 3—hydrogeology Resources, New Mexico Institute of Mining and regional deformation event. Discordant dikes Technology, Socorro, New Mexico 87801 A SALINIZATION STUDY WITHIN THE SAN and stocks of pegmatitic alkali granite intruded We have prepared a map of the regional water ACACIA REGION, SEVILLETA NATIONAL the other units. The pegmatites are megacrys- table in the southern Sacramento Mountains WILDLIFE REFUGE (SNWR), NEW MEXI- tic with a preponderance of alkali feldspar and based on measurements made in water wells in CO, F. Reyes, [email protected], Depart- quartz. All of the granitic phases are nearly March 2008 and elevations of flowing springs ment of Environmental Sciences, University of saturated with respect to alumina. The granitic and gaining reaches of streams. The aquifer sys- Texas at El Paso, El Paso, Texas 79968; S. Adel- sheets and foliated granite have overlapping tem in the southern Sacramentos is developed berg, Department of Geological Sciences, Brown major and trace element values, while the peg- primarily within the Yeso Formation, a hetero- University, Providence, Rhode Island 02912; matites have higher weight percent SiO , higher geneous unit composed of siltstone, mudstone, 2 A. Williams, L. J. Crossey, and K. E. Karlstrom, elemental Ba and Rb, and lower elemental Zr gypsum, and fractured limestone. Water-bearing Department of Earth and Planetary Sciences, and Zn. The Hermit’s Peak batholith is located zones are distributed throughout the section. The University of New Mexico, Albuquerque, New in the transition zone between the Yavapai and system is recharged near the crest of the Sacra- Mexico 87131 Mazatzal Precambrian provinces. Radiometric mentos where high mountain springs discharge age determinations are needed to constrain the The arid climate of the American Southwest from small, highly localized perched aquifers. timing of magmatism and fabric development poses concerns in water management for both Stream flow derived from these springs re-enters and help resolve whether the Mazatzal orogeny ground and surface waters in the Rio Grande the ground water system along losing reaches was a discrete or protracted tectonic event. rift corridor. High salinity and elevated trace ele- and may “daylight” multiple times along the ment concentrations tend to impair water qual- flowpath, feeding springs at lower elevations. In ity; hence identifying sources of these contami- most cases it is impossible to determine whether nants remains an important ongoing challenge. a measured water level corresponds to a perched MODELING PYRITE AND FLUORIDE CON- Geochemical studies show an increase in salinity aquifer or is part of the regional piezometric sur- CENTRATION IN THE GOATHILL NORTH in the Rio Grande near San Acacia, located at the face, and the distinction is probably irrelevant at ROCK PILE, QUESTA MINE, NEW MEX- southern end of the Albuquerque Basin. Alter- the scale of observation of the entire watershed. ICO, S. F. Williams, [email protected], nate models contend that: (1) deep-seated faults The regional hydraulic gradient is steepest near New Mexico Bureau of Geology and Mineral within the rift provide conduits for the ascent the crest of the Sacramentos, and progressively Resources, New Mexico Institute of Mining of deeply derived saline fluids, and (2) upwell- decreases to the east. Locally steeper gradients and Technology, Socorro, New Mexico 87801 ing of sedimentary basin brines takes place at also occur in the vicinity of major faults. More broadly spaced water level contours at lower The New Mexico Bureau of Geology and Mineral interbasin constrictions. We used aqueous geo- elevations in the Sacramentos probably reflect Resources recently took part in an elaborate study chemical techniques (field parameters, major 18 mounding of the water table in areas where the called the Questa Rock Pile Weathering and Sta- and trace elements, Cl/ Br ratios, δδ O and δD) and geochemical modeling to identify salinity aquifer is recharged through sinkholes and karst bility Project. The purpose of this project was to components in the middle Rio Grande basin. An fissures. Because eastward stratigraphic dip is determine how and to what extent weathering integrated study of spring geochemistry centered greater than the regional hydraulic gradient, east affects the gravitational stability of the Questa at the SNWR with factors related to poor water of the Six-Mile buckle the aquifer system is devel- mine rock piles over time periods on the order of quality will allow for an improved comprehen- oped in karstic limestones of the San Andres For- hundreds to thousands of years. During the peri- sion of natural contaminants in the Rio Grande mation rather than the Yeso. The higher transmis- od of open pit mining (1969–1982) at the Questa hydrochemical system. Results show that the Rio sivity of the San Andres Limestone is reflected in mine, several million tons of overburden rock was Salado Box (RSB) and San Acacia (SA) springs are a pronounced flattening of the water table as the removed and deposited into rock piles on moun- both major salinity inputs. SA contains the high- southern Sacramentos aquifer merges with the tain slopes and into valleys. Since the emplace- est salinity concentrations of all SNWR waters, artesian aquifer of the Roswell Artesian Basin. ment of these rock piles, several minor slumps and it is observed to influence the nearby canals. Water level change maps show that during the have occurred as well as a foundation failure at The increase in salinity in the Rio Grande appears period from 2006 to 2007 water levels in the high Goathill North (GHN) rock pile. This slide was to be caused by SA springs and its evaporative Sacramentos began rising in response to unusu- halted and GHN made stable by removing mate- pools. Major ion, stable isotope, and trace element ally intense monsoonal rains in fall, 2006. Water rial from the top and relocating it to the bottom analyses suggest that SA is chemically similar to levels continued to rise in the subsequent two forming a buttress. The regraded GHN provid- the RSB waters and that the SA brine pool has years, but the center of greatest increase migrat- ed a rare opportunity to examine, sample, and evolved through evaporative concentration. RSB ed progressively farther to the east, suggesting develop a conceptual model of the undisturbed has been established as having deeply derived that the 2006 monsoon event was continuing to interior of a large mine rock pile in situ. During fluid sources based on He isotopic data. We con- be felt as an eastward diffusion of pressure head this process, several hundred parameters were clude that rift-bounding and intra-rift basement- through the aquifer system. measured, tested, and observed. Specifically, this penetrating faults can provide “fast paths” for the poster describes the techniques used to model the ascent of saline fluids. These endogenic waters Poster session 4—geophysics distribution of pyrite and fluoride concentration are potentially influenced by relatively small and structure within the rock pile. volumes of upwelling fluids through granitic Modeling was performed using the Geo- basement (with associated increases in F, Li, and PALEOMAGNETIC DATA FROM LATE MIO- statistical Analyst Extension in ESRI’s ArcGIS Ba) and the Socorro Magma Body (excess CO2). CENE LOBATO BASALT FLOWS ADJA- (version 9.3.1) software. The models used were: Within the SA region there are numerous springs CENT TO THE SANTA CLARA FAULT SYS- Inverse Distance Weighting, Global Polynomial that are all potential fault-controlled endogenic TEM, CHILI QUADRANGLE, RIO ARRIBA Interpolation, Local Polynomial Interpolation, fluid sources. Salinity sources that contribute to COUNTY, NEW MEXICO, M. S. Petronis, and Radial Basis Functions. It was found that the salinization of the Rio Grande through fault [email protected], and J. Lindline, Environ- both Inverse Distance Weighting and Radial conduits at San Acacia degrade the water qual- mental Geology Program, Natural Resource Basis Functions produced realistic models ity of the Rio Grande and its aquifers, posing a Management Department, New Mexico High- while Global Polynomial Interpolation and hazard to downstream users. lands University, Las Vegas, New Mexico 87701

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 69 The Late Miocene Lobato Formation comprises and susceptibility contrasts between the various Tributary alluvial fans in the lower Chama River predominantly fine-grained and vesicular oliv- formations within the basin. Gravity and mag- canyon, in northern New Mexico between Christ ine- and plagioclase-phyric alkaline basalts. netic data were modeled along several regional in the Desert Monastery and Big Eddy boat ramp Lobato volcanism represents some of the pre- profiles on selected parts of the Galisteo Basin, north of Abiquiu Reservoir, affect the main chan- caldera mafic volcanism in the Jemez Mountain combined with surface geologic information, to nel form and slope of the Chama River in various volcanic field and coincided with an episode constrain the nature of the subsurface. Both sets ways. Some fans deposit bouldery debris flows of crustal extension in the Española Basin. We of potential field data were integrated into Arc- into the river, creating rapids. Other fans deposit examined a 100-m-thick sequence of the Loba- GIS 9.3 and Surfer 8.0 to generate extrapolated large volumes of sandy sediment, in some cases to Formation on the north side of Arroyo de la surfaces and derivative maps that allowed for pushing the river to the opposite side of the val- Plaza Larga Canyon. Here, the Lobato flows the characterization of the subsurface geology ley. The purpose of this study is to determine the are subhorizontal to gently dipping for nearly along specific profiles across the mapped area. controls on alluvial fan size, morphology, and 2 km southeast from the Cerro Roman volcanic These data reveal that several anomalies exist sediment texture that result in these differences. center, then dip steeply about a roughly north- within the central portion of the basin that we Most tributaries have cut channels into their west-trending axis, then abut and dip modestly interpret as likely hydrocarbon trap-structures. fans, creating exposures of the fan stratigraphy. against the Santa Clara fault—a major structure In order to investigate the possible geometries of Sample sites along the length of each tributary on the western margin of the Española Basin. the anomalies, detailed forward models are being channel were used to determine particle-size dis- We studied the disposition of these lava flows developed to assess possible trap structures, tribution, from which the median particle size, and attempted to distinguish between (1) lava extent, and distribution within the basin. These sorting, and other measures where derived. In the flow emplacement into a paleovalley that existed data should allow us to estimate the hydrocar- field, the fan boundaries and channel boundaries in the late Miocene along the Santa Clara fault bon potential within select parts of the basin and were mapped. Digital elevation models (DEMs) system or (2) post-emplacement drag folding provide an estimate of reserves present. were used in ArcGIS to delineate the drainage against the Santa Clara fault. Paleomagnetic data basins for each fan, the area, relief, and slope were collected from 16 sites along a transect rep- angles of the drainage basins, and the area and resenting the arcuate structure in order to con- slope of the fans. ArcGIS was also used to deter- duct a paleomagnetic fold test. Remanent mag- ORIGIN AND TIMING OF FOLDING WITH- mine each geologic unit's role on particle size and netizations were measured using a AGICO JR6-A IN THE LINCOLN FOLD BELT, LINCOLN Dual-Speed magnetometer at the New Mexico COUNTY, NEW MEXICO, T. B. Avant, and distribution on fan; in the study area the geologic Highlands University paleomagnetic-rock mag- J. M. Amato, Department of Geological Scienc- units include Triassic Chinle Group through Cre- netic laboratory. Specimens were progressively es, New Mexico State University, Las Cruces, taceous Dakota Formation sedimentary rocks. AF demagnetized in 10–15 steps to a maximum New Mexico 88003 Drainage basin area, stream length, and stream field of 120 mT to isolate the geological impor- The Lincoln fold belt contains a set of disharmon- magnitude have a significant impact on particle tant characteristic remanent magnetization. ic, short wavelength folds with a controversial size on fan. Larger area, longer length, and high- Paleomagnetic data reveal a single component timing and origin. Located just outside the vil- er magnitude produce larger mean particle sizes magnetization that decays to the origin with less lage of Lincoln, New Mexico, folded sedimentary on fans. The ratio between fan size and drainage than 10% of the natural remanent magnetization rocks of the Leonardian (middle Permian) Yeso basin size also appears important. Smaller fans remaining after treatment in 120 mT fields. In Formation are exposed in the surrounding hills. tend to have less fining of clast size down fan, situ results from sites located in the subhorizon- The overlying Permian San Andres Formation is especially if their drainage basin is large in com- tal hinge zone and those from the east fold limb poorly exposed and contains harmonic folds with parison with fan area. These fans produce boul- yield statistically indistinguishable remanence long wavelengths. Both of these units are located dery debris flows into the river. Large fans, espe- directions. Following structural correction based in an area with a complex geologic history. cially if their drainage basin is relatively small, on the strike and dip of the individual flows, the Previous stratigraphic and structural studies have more down-fan fining of particle size. In dispersion between the two data sets increases, resulted in several possible mechanisms and some cases these fans redirect the river channel indicating a negative paleomagnetic fold test. We ages of fold formation being proposed. Estimates with large volumes of sandy sediment. argue that the lava flows were emplaced into a of the age of fold formation range from Permian Bedrock geology appears to have a strong influ- paleovalley of considerable relief adjacent to the (syndepositional) to Tertiary. Proposed mecha- ence on the fan's particle size, where a greater percent area of Dakota Formation produces abun- Santa Clara fault during the late Miocene. These nisms for the formation of the folds include soft- dant boulders and a larger mean particle size. data indicate that the Santa Clara fault was a sediment deformation, gravitational mass wast- Morrison Formation and Entrada sandstones tend prominent structure that influenced the paleo- ing and slumping, Laramide deformation, defor- topography of the western margin of the Rio to weather by granular disintegration, and along mation caused by the dikes and sills from either Grande rift in the late Miocene. with Petrified Forest Formation mudstones, pro- the nearby Capitan pluton or the Sierra Blanca duce overall smaller particle sizes. intrusion, and deformation caused by movement along basement faults. GEOPHYSICAL DATA BEARING ON Mapping of the study area has yielded bed- GEOCHRONOLOGY, GEOCHEMISTRY, HYDROCARBON TRAPS AND RESOURCE ding measurements within the Yeso Formation AND TECTONIC OCCURRENCE OF TRAV- POTENTIAL OF THE GALISTEO BASIN, that strike predominantly northwest/southeast, ERTINE DEPOSITS IN NEW MEXICO AND NEW MEXICO, R. A. Ashu, aragbor@yahoo. and fold axes that trend predominantly north- ARIZONA, A. Priewisch, [email protected], com, and M. S. Petronis, Environmental Geol- east/southwest. Wavelength measurements in L. J. Crossey, E. Embid, and K. E. Karlstrom, ogy, Natural Resource Management Depart- the Yeso folds range from 10 to 60 m. Fold trends Department of Earth and Planetary Sciences, ment, New Mexico Highlands University, Las do not vary significantly with distance measured University of New Mexico, Albuquerque, New Vegas, New Mexico 87701 perpendicular to the fold axes. Bedding within Mexico 87131 the overlying San Andres does not appear to have Land-based gravity and magnetic data were CO springs and associated travertine deposits obtained at 56 gravity and 250 magnetic stations a consistent strike pattern, but all fold axis mea- 2 offer a unique tool to better understand Ceno- throughout the northern to central Galisteo Basin surements trend north to northeast. Wavelengths zoic paleohydrology, paleoclimate, and tecton- south of Santa Fe, New Mexico. The study area in San Andres folds range from 300 to 400 m. The ics. Travertine accumulations represent places extends south from the village of Eldorado to the Yeso–San Andres contact is discordant, possibly of persistent and significant mantle CO degas- foothills of the Ortiz Mountains and east from due to the presence of an unconformity or fault. 2 I–25 to Highway 285; an area of approximately U-Pb dating of crosscutting diabase dikes will be sing linked to their tectonic environment. Their 3,600 km2. These data provide a novel approach used to better constrain the timing of folding. geochemistry records paleohydrology and in subsurface investigations by integrating sur- paleoclimate, and hence precise dates on these face geological mapping and subsurface geo- poster session 5—Alluvial fans rocks offer a productive venue for evaluating physical surveys to characterize the geometry, and travertine deposits Cenozoic tectonic and climate histories. Recent distribution, depth, and potential hydrocarbon U/Th dates from Springerville, Arizona, show trap geometries in parts of the Galisteo Basin in CONTROLS ON PARTICLE-SIZE DISTRIBU- that: (1) travertine deposition began before 2.5D using the Talwani and GravMag geophysi- TIONS IN TRIBUTARY ALLUVIAL FANS 350 ka, with major accumulations occurring in cal modeling softwares and field exploration OF THE LOWER CHAMA RIVER CANYON, cycles of approximately 70 ka; (2) the CO2 of methods. The structurally complex nature of J. Faulconer, [email protected], and G. A. modern travertine-depositing springs is partly the Galisteo Basin provides an excellent location Meyer, Department of Earth and Planetary Sci- derived from the mantle based on 3He/4He and 3 for stratigraphic and structural trap exploration ences, University of New Mexico, Albuquer- CO2/ He ratios; and (3) incision rates of the using geophysical methods due to the density que, New Mexico 87131 Little Colorado River increased markedly in the

70 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 last 100 ka. On-going work at Mesa Aparejo and efflorescent surface accumulations, which are from Alamogordo on the west to Dunken on Mesa del Oro, New Mexico, reveals similar large periodically removed by re-dissolution and the east, and from the southern border of the magnitude, but less-studied, travertine deposits. wind deflation. Mescalero Apache Reservation to the north- Proposed research methods involve radiogenic The uncommon surficial features related to ern border of McGregor Military Range. The isotope geochemistry for U-series dating of the accumulation by gypsum precipitation include compilation comprises new mapping from the travertine, stable isotope geochemistry to evalu- megamounds, meandering raised-levee streams, Statemap program, mapping funded under ate biogenic influences and paleoclimate/paleo- platform marshes, raised-rim marshes, and hum- the Sacramento Mountains hydrogeology study, hydrology fluctuations, geochemical analysis mocky rolling plains that appear to represent and existing mapping by Pray (1961) along the with XRF and electron microprobe, a detailed modification of previously deposited gypsum western escarpment and Black (1973) near Piñon. petrographic study, mapping, and GIS analysis. by eolian and/or dissolutional processes. It covers approximately 24 7.5-min quadrangles The data of the three locations will be compared, never before mapped at 1:24,000-scale. systematically analyzed, and put into context The important units exposed over the major- with the paleohydrology, paleoclimatology and GEOLOGIC COMPILATION MAP OF THE ity of the map area are the Permian Yeso and San neotectonic processes of the Rio Grande rift–Col- LOWER PECOS ALLUVIAL VALLEY, BIT- Andres Formations. The Yeso Formation consists orado Plateau region. TER LAKE TO BOTTOMLESS LAKES AREA, of red and yellow siltstones and mudstones, and CHAVES COUNTY, NEW MEXICO, D. J. gray carbonates. It is exposed, generally poorly, McCraw, [email protected], New Mexico Bureau along valley bottoms and lower valley walls poster session 6—geologic mapping of Geology and Mineral Resources, New Mexi- throughout the north-central part of the map area, and spatial archeology co Institute of Mining and Technology, Socorro, along the upper flanks of the western escarpment New Mexico 87801 and in the Sacramento River drainage, and in iso- PRELIMINARY GEOLOGIC MAP OF THE lated outcrops in the southeast. Springs are very A recent compilation of NMBGMR-STATEMAP CAPITOL PEAK SE QUADRANGLE WITH common below the contact between the Yeso and geologic mapping of the Bitter Lake, South ILLUSTRATIONS OF UNCOMMON SURFI- San Andres Formations. Following Kelley (1971), Spring, and Bottomless Lakes 7.5-min quadran- CIAL FEATURES, NORTHERN TULAROSA three members of the San Andres Formation were gles in the lower Pecos valley depicts a late Pleis- BASIN, SOUTH-CENTRAL NEW MEXICO, mapped, except in the highest elevations, where tocene–Holocene floodplain, flanked to the west D. W. Love, [email protected], New Mexico exposures are poor and vegetation precluded by Plio–Pleistocene alluvial terraces, dissected Bureau of Geology and Mineral Resources, aerial photo identification. by the Arroyo Hondo. These are cut into Perm- New Mexico Institute of Mining and Technol- Major structures are (1) the Tertiary Alamog- ian limestone of the San Andres Formation to the ogy, Socorro, New Mexico 87801; B. D. Allen, ordo fault, along which the east-tilted mountain west, overlain by the thick evaporite sequence of New Mexico Bureau of Geology and Mineral block was uplifted; (2) the Tertiary Sacramento the Artesia Group. The extensive gypsum beds of Resources–Albuquerque Office, New Mexico River fault zone, composed of west-side-down, Institute of Mining and Technology, Albuquer- the Seven Rivers Formation, riddled with karstic southeast-trending normal faults that define the que, New Mexico 87106; and R. G. Myers, U.S. depressions and sinkholes, underlie the valley Sacramento River drainage; (3) the southern ter- Army, IMWE-WSM-PW-E-ES, White Sands and form the eastern bluffs of the valley margin. mination of the Dunken–Tinnie anticlinorium, a Missile Range, New Mexico 88002 Many of these sinks serve as conduits for numer- north-south zone of tight folding and associated ous springs derived from the underlying artesian Near the northernmost floor of the Tularosa Basin, faults with variable dip-slip and possible strike- aquifer, and are oriented roughly parallel to or the demarcated Capitol Peak SE 7.5-min quad- slip motion; and (4) the southwestern termina- orthogonal to the southwest-northeast-trending rangle is at the junction of three drainages (Car- tion of the Six-Mile and Y-O buckles, right-lateral regional structural buckles. rizozo valley, upper Salt Creek–Mound Springs, strike-slip faults that cross the Pecos Slope. The Three alluvial terraces are mapped west of the and Three Rivers fan) and a western piedmont latter three structures are only constrained to be Pecos valley: remnants of the Plio–Pleistocene slope. This junction, along with an uncommon, younger than Permian in age. Complex faults and sulfate-precipitating planar wetland, created a Blackdom terrace, the broad mid-late Pleisto- folds in the southeast probably resulted from the low-gradient surface that stalled the Carrizozo cene Orchard Park terrace, and the late Pleisto- interaction of Tertiary block-faulting with exist- lava flow. Burned grasses buried at the snout of cene Lakewood terrace. The inset modern Pecos ing northeast-trending basement structures. We the lava flow in the quadrangle yielded an ages of floodplain, reaching a maximum thickness of interpret the northeast–trending segment of the ~ 45 m along the western margin, is comprised 4,680 ± 40 radiocarbon yrs b.p. (Beta-277075; Cal Rio Peñasco near Mayhill to be a fault, and it is a of late Pleistocene braided stream deposits, and b.p. 5,480–5,310 with 95% probability). The flow hydrologically significant boundary. overrode alluvium and a complex environment of three Holocene meanderbelts. A series of col- evaporite deposition and eolian features. In turn, lapse depressions, extending roughly 14 km on these contrasting depositional processes contin- the eastern valley margin, also contain late Pleis- NATIVE AMERICAN LITHIC PROCURE- ued after the lava flow and buried its margins tocene–middle Holocene Pecos River alluvium. MENT PATTERNS AND SITES IN THE and kipukas by up to 3 m of alluvial, evaporite, The Arroyo Hondo has built extensive fans BOOTHEEL OF SOUTHWESTERN NEW and loessal sediments. Post-lava alluvium accu- onto the Orchard Park terrace throughout the MEXICO, K. E. Zeigler, zeiglergeo@gmail. mulates on top of several types of ground water- Pleistocene. Gravel pits in Arroyo Hondo fan com, ZGC, Albuquerque, New Mexico, 87123; discharge gypsum and has spread out across the deposits exhibit decreasing pedogenic carbon- C. Hughes, A. Kurota, and P. Hogan, Office of north-central part of the quadrangle. To the west, ate development from south to north, imply- Contract Archeology, University of New Mexi- the broad valley of Salt Creek is incised up to 13 ing a northward shift of the river to its present co, Albuquerque, New Mexico 87131 entrenched channel. A large late Pleistocene dis- m below the level of maximum basin fill. The val- Multidisciplinary field projects can be very use- ley borders of Salt Creek consist of sparse, wind- tributary fan pushed the Pecos River eastward into the collapse depressions, allowing the ear- ful to a more fundamental understanding of the deflated basin-fill exposures of fine-grained clas- world around us, though these projects are not as ly-middle Holocene Arroyo Hondo to build its tic and gypsic beds and crossbedded pebbly sand common as they should be. In particular, the com- first two of three meanderbelts across the entire channels, and moist fine-grained alluvial/eolian bination of archeology and geology combines our Pecos floodplain. Two Pecos River meanderbelts slopes where ground water seeps just below the understanding of human behavior and human have since cut through these Rio Hondo alluvial surface. The southwestern quarter of the quad- use of the landscape with an intimate knowledge rangle consists of a complex string of marshes, deposits. of geologic processes and the materials available playas, blowouts, eolian dunes, and alluvial chan- for human use in order to gain a broader under- nels with discontinuous outcrops of basin fill. standing of human-Earth interaction. Here we Stripped exposures of basin fill exhibit rare track- GEOLOGIC MAP OF THE SOUTHERN SAC- present data from a cross-disciplinary project that ways of Pleistocene megafauna (proboscideans?). RAMENTO MOUNTAINS, OTERO AND uses a common dataset, archeological artifacts, to Evidence of subsurface dissolution includes karst CHAVES COUNTIES, NEW MEXICO, G. C. explore the anthropological and geologic impli- features and tilted basin fill. Rawling, [email protected], New Mexico cations of useage patterns. Archeological exca- The two endemic populations of White Sands Bureau of Geology and Mineral Resources– vations and surveys conducted by the Office of pupfish (Cyprinodon tularosa) live in Salt Creek Albuquerque Office, New Mexico Institute of Contract Archeology in 2007 along the route of and Malpais Spring and salt marsh on the quad- Mining and Technology, Albuquerque, New the proposed international border fence reveal rangle. In addition to gypsum, the modern Mexico 87106 patterns of use of geologic materials by Archaic, brackish-to-saline springs, streams, and wetland The NMBGMR has recently completed a new Formative, and Protohistoric Native Americans environments precipitate halite, hexahydrite, 1:100,000-scale geologic map of the southern Sac- in the bootheel of southwestern New Mexico. thenardite, and other soluble salts as widespread ramento Mountains. The mapped area extends Thousands of artifacts were recorded in multiple

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 71 sites from Guadalupe Pass in the southern Pelon- native peoples are local siliceous volcanic materi- pre-Spanish site and one post-Spanish site that are cillo Mountains to the Carrizalillo Hills west of als. However, several artifacts constructed from adjacent to one another. Columbus. We identified the lithologies of arti- obsidian were transported into the region from facts, ranging from projectile points to ground- northern Mexico and eastern Arizona, indicat- stones, and then constructed material movement ing long-distance travel and/or trade routes. We New Mexico Geology thanks the New Mexi- maps based on either known procurement sites also examine useage pattern difference between co Geological Society Foundation for their (“quarries”) or outcrops identified as the closest Archaic, Formative, and Protohistoric sites. Addi- continuing financial support of the publica- source to a given site for each lithology. Not unex- tionally, a dramatic change in distribution of tion of these abstracts. pectedly, the majority of the rock types utilized by sources for geologic materials occurs between one

NMGS spring meeting Student winners for best presentation

18 Each year a panel of judges evaluates student oral and poster presen- δ O, and trends in εεNd.” Two students tied for best poster presenta- tations. Scores are tallied from judging forms. This year the award for tion: Francisco Reyes for “Salinization study within the San Acacia best student talk was given to Bethany Theiling for her presentation region, Sevilleta National Wildlife Refuge (SNWR), New Mexico” “Insights into the relationship between continental weathering and and Joshua Faulconer for “Controls on particle-size distributions in high-frequency (104–105 yr) glacio-eustasy from cyclostratigraphy, tributary alluvial fans of the lower Chama River canyon.”

NMGS abstracts author index

Adelberg, S., p. 69 Fellah, K., p. 63 Kurota, A., p. 71 Priewisch, A., p. 70 Allen, B. D., pp. 66, 71 Ferguson, C., p. 63 Land, L., pp. 61, 69 Rawling, G. C., pp. 60, 61, 69, 71 Amato, J. M., pp. 63, 70 Fernald, A., pp. 62, 65 Lawrence, J. R., p. 63 Reyes, F., p. 69 Ashu, R. A., p. 70 Finch, S. T., p. 61 Lerner, A. J., pp. 63, 66, 68 Riesterer, J., p. 65 Asmerom, Y., p. 64 Garduño, H., p. 62 Lindline, J., pp. 68, 69 Rinehart, L. F., pp. 65, 67 Avant, T. B., p. 70 Geissman, J. W., p. 64 Longrich, N. R., p. 66 Sealey, P. L., p. 67 Barrick, J. E., p. 66 Goff, C. J., p. 63 Love, D. W., pp. 64, 71 Shukla, M., pp. 62, 65 Bemis, K., p. 65 Goff, F., pp. 60, 63 Lucas, S. G., pp. 63–68 Smith, G. A., p. 64 Berman, D. S., p. 67 Guldan, S., p. 65 MacDonald, J. P., p. 68 Spielmann, J. A., pp. 63, 65–68 Bleisweiss, M., p. 65 Gutzler, D. S., p. 64 McCraw, D. J., p. 71 Sullivan, R. M., p. 67 Bourdon, J., p. 68 Harris, S. K., pp. 65, 67, 68 McIntosh, W. C., pp. 63, 64 Sturgis, J., p. 64 Braman, D. R., p. 67 Heizler, L. L., p. 63 McKeighen, H. W., p. 65 Timmons, S. S., pp. 61, 62, 69 Bright, R. M., p. 63 Henrici, A. C., p. 67 McKeighen, Jr., K. L., p. 65 Theiling, B., p. 64 Cather, S. M., p. 64 Hogan, P., p. 71 Meyer, G. A., p. 70 Vachard, D., p. 66 Connell, S. D., p. 64 Hughes, C., p. 71 Myers, R. G., p. 71 Vanleeuwen, D., p. 62 Cron, B., p. 60 Hunt-Foster, R. K., p. 66 Newton, B. T., pp. 61, 62 Williams, A., p. 69 Crossey, L. J., pp. 60, 69, 70 Jasinski, S. E., p. 67 Northup, D. E., p. 60 Williams, S. F., p. 69 Drakos, P., p. 65 Karlstrom, K. E., pp. 60, 69, 70 Osburn, G. R., p. 63 Williamson, T. E., p. 66 Dunbar, N. W., pp. 63, 64 Kelley, S. A., pp. 60, 63 Partey, F. K., p. 61 Wolff, J. A., p. 63 Durney, K., p. 68 Kempter, K. A., p. 60 Pence, R., pp. 67, 68 Wright, K., pp. 67, 68 Elrick, M., p. 64 Klein, H., p. 63 Peters, L., p. 60 Zeigler, K. E., pp. 60, 62, 71 El-Sadek, A., p. 65 Kludt, T., pp. 61, 62 Petronis, M. S., pp. 69, 70 Embid, E., p. 70 Koning, D. J., p. 60 Pitrucha, R. M., p. 68 Faulconer, J., p. 70 Krainer, K., pp. 64, 66, 68 Polyak, V., pp. 61, 64

NMGS abstracts subject index

Abo Formation, McKeighen, H. W., et al., p. 65; McKeighen, K. L., et al., p. 65 geochronology Albuquerque Basin, Connell et al., p. 64 Ar/Ar Bernalillo County Albuquerque Basin, Connell et al., p. 64 Upper Cretaceous shark assemblage, Pence et al., p. 67; Wright et al., p. 68 Mount Taylor, Goff et al., p. 63 Burro Mountains, Bright and Amato, p. 63 magnetostratigraphy, see paleomagnetism tephrochronology Chama River, Faulconer and Meyer, p. 70 Albuquerque Basin, Connell et al., p. 64 Chinle Group U-Pb zircon fossil plants, Lucas and Spielmann, p. 66 Salt River Canyon (Arizona) dike, Bright and Amato, p. 63 Redonda Formation vertebrate ichnofossils, Spielmann et al., p. 63 U-Th climate Snowy River formation (Fort Stanton Cave), Land et al., p. 61 glacial-interglacial cycles, Theiling et al., p. 64 Springerville (Arizona) travertine deposits, Priewisch et al., p. 70 Middle Pennsylvanian, Theiling et al., p. 64 geomorphology North American monsoon, Sturgis and Gutzler, p. 64 particle-size distribution in tributary alluvial fans, Faulconer Doña Ana County and Meyer, p. 70 Cerro de Cristo Rey, Krainer et al., p. 68 Sacramento Mountains-derived alluvial fans, Koning, p. 60 geophysics Prehistoric Trackways National Monument, Lerner et al., p. 68 gravity and magnetic surveys Galisteo Basin, Ashu and Petronis, p. 70 Galisteo Basin, Ashu and Petronis, p. 70 geoarchaeology, Zeigler et al., p. 71 Gray Mesa Formation, Theiling et al., p. 64 geochemistry ground water CO2-rich travertine-depositing springs, Cron et al., p. 60 CO2-rich travertine-depositing springs, Cron et al., p. 60; Mount Taylor pyroclastic eruptions, Dunbar et al., p. 63 Priewisch et al., p. 70

72 Ne w Me x i c o Ge o l o g y May 2010, Volume 32, Number 2 southern Sacramento Mountains, Finch, p. 61; Land et al., p. 69; petrology Newton et al., p. 61; Rawling, p. 60; Timmons et al., p. 61; Hermit's Peak batholith, Pitrucha and Lindline, p. 68 Zeigler et al., p. 62 Proterozoic springs on Zuni tribal lands, Drakos et al., p. 65 diabase dikes and sills, Bright and Amato, p. 63 Hidalgo County Hermit's Peak batholith, Pitrucha and Lindline, p. 68 geoarchaeology, Zeigler et al., p. 71 Redonda Formation, Spielmann et al., p. 63 hydrochemistry Rio Arriba County CO2-rich travertine-depositing springs, Cron et al., p. 60 Cañon del Cobre, Harris et al., p. 68; Spielmann et al., p. 67 Snowy River formation (Fort Stanton Cave), Land et al., p. 61 fossil reptiles, Harris et al., p. 68; Spielmann et al., p. 67 southern Sacramento Mountains, Newton et al., p. 61; Rawling, p. 60; Rio Grande Timmons et al., p. 61 salinization study, Reyes et al., p. 69 hydrogeology Robledo Mountains Formation, Lerner et al., p. 68 southern Sacramento Mountains, Zeigler et al., p. 62 Rowe–Mora Basin, Rinehart and Lucas, p. 65 hydrology Sacramento Mountains effects of tree thinning on water yields, Garduño et al., p. 62; alluvial-fan deposits, Koning, p. 60 Newton et al., p. 62 effects of tree thinning on hydrology, Garduño et al., p. 62; modeling of ungaged watersheds, El-Sadek et al., p. 65 Newton et al., p. 62 North American monsoon, Sturgis and Gutzler, p. 64 geologic map, Rawling, p. 71 Sacramento Mountains watershed study, Garduño et al., p. 62; hydrogeology, Rawling, p. 60 Land et al., p. 69; Newton et al., p. 62 ion chemistry of springs and well water, Timmons et al., p. 61 Jemez Mountains perched ground water system, Finch, p. 61 Lobato basalt flows, Petronis and Lindline, p. 69 Sierra Blanca, Kelley et al., p. 60 Lincoln County stable isotopic compositions of natural waters, Newton et al., p. 61 Fort Stanton Cave, Land et al., p. 61 volcanic stratigraphy, Kelley et al., p. 60 Lincoln fold belt, Avant and Amato, p. 70 water table map, Land et al., p. 69 Lobato Formation, Petronis and Lindline, p. 69 Yeso Formation, Zeigler et al., p. 62 Madera Group San Andres Formation, Avant and Amato, p. 70 Atrasado Formation, Lucas et al., p. 66 Sandoval County Mancos Shale Mesa Prieta ammonites, Sealey and Lucas, p. 67 ammonites, Sealey and Lucas, p. 67 Tierra Amarilla anticline, Cron et al., p. 60 Manzano Mountains, Lucas and Krainer, p. 64 Sangre de Cristo Formation, Rinehart and Lucas, p. 65 maps San Juan Basin Capitol Peak SE 7.5-min quadrangle, Love et al., p. 71 Cretaceous palynomorph assemblage, Sullivan et al., p. 67 lower Pecos alluvial valley compilation, McCraw, p. 71 Pentaceratops quarry, Hunt-Foster et al., p. 66 southern Sacramento Mountains, Rawling, p. 71 San Miguel County Mesaverde Group Hermit Peak, Pitrucha and Lindline, p. 68 Point Lookout Sandstone, Pence et al., p. 67; Wright et al., p. 68 sedimentology Molycorp molybdenum mine, Williams, p. 69 particle-size distribution in tributary alluvial fans, Faulconer and Mount Taylor, Dunbar et al., p. 63; Goff et al., p. 63 Meyer, p. 70 Sevilleta National Wildlife Refuge, Reyes et al., p. 69 Organ Mountains, Bright and Amato, p. 63 Sierra County paleomagnetism Mud Springs Mountains, Lucas et al., p. 66 Albuquerque Basin (Plio–Pleistocene), Connell et al., p. 64 speleogenesis Lobato Formation, Petronis and Lindline, p. 69 Fort Stanton Cave, Land et al., p. 61 paleontology stratigraphy Abo Formation, McKeighen, H. W., et al., p. 65; Albuquerque Basin magnetic-polarity stratigraphy (Plio–Pleistocene), McKeighen, K. L., et al., p. 65 Connell et al., p. 64 ammonites (Turonian), Sealey and Lucas, p. 67 Cerro de Cristo Rey Cretaceous depositional environments, Cretaceous palynomorph assemblage, Sullivan et al., p. 67 Krainer et al., p. 68 dinosaurs, Sullivan et al., p. 67 Kinney quarry, Lucas et al., p. 66 fossil plants, Lucas and Spielmann, p. 66 Manzano Mountains Pennsylvanian strata, Lucas and Krainer, p. 64 Kinney quarry, Lucas et al., p. 66 Mount Taylor pyroclastic eruptions, Dunbar et al., p. 63 Pentaceratops quarry, Hunt-Foster et al., p. 66 structural geology Permian nonmarine bivalves, Rinehart and Lucas, p. 65 Lincoln fold belt, Avant and Amato, p. 70 Prehistoric Trackways National Monument, Lerner et al., p. 68 Santa Clara fault, Petronis and Lindline, p. 69 Redonda Formation vertebrate ichnofossils, Spielmann et al., p. 63 Taos County Robledo Mountains Formation invertebrate ichnofossils, Lerner et al., p. 68 Molycorp molybdenum mine, Williams, p. 69 Sangre de Cristo Formation, Rinehart and Lucas, p. 65 Torrance County selachians, Pence et al., p. 67; Wright et al., p. 68 Abo Pass, McKeighen, H. W., et al., p. 65; McKeighen, K. L., et al., p. 65 synapsid reptiles, Harris et al., p. 68; McKeighen, H. W., et al., p. 65; travertine, Cron et al., p. 60; Priewisch et al., p. 70 McKeighen, K. L., et al., p. 65; Spielmann et al., p. 67 Tularosa Basin, Koning, p. 60; Love et al., p. 71 Zoophycos burrows, Lucas et al., p. 66 volcanology Pecos valley, McCraw, p. 71 Hermit's Peak batholith, Pitrucha and Lindline, p. 68 Pennsylvanian Lobato basalt flows, Petronis and Lindline, p. 69 glacio-eustasy, Theiling et al., p. 64 Mount Taylor, Dunbar et al., p. 63; Goff et al., p. 63 Manzano Mountains lithostratigraphy, Lucas and Krainer, p. 64 Sierra Blanca volcanic field, Kelley et al., p. 60 petroleum and natural gas Yeso Formation, Avant and Amato, p. 70; Zeigler et al., p. 62 Galisteo Basin, Ashu and Petronis, p. 70 Zuni Pueblo, Drakos et al., p. 65

May 2010, Volume 32, Number 2 Ne w Me x i c o Ge o l o g y 73