Horace Springs is the start of a perennial reach of the Rio San Jose at the Pueblo of Acoma, New Mexico. As the meandering Rio San Jose flows through a gap between Horace Mesa to the north and La Ventana Mesa to the south, the alluvial aquifer system lies in the gap, causing a decrease in the alluvial aquifer’s cross-sectional area resulting in groundwater discharging to the streambed. Horace Springs, currently, discharges about 3.5 to 4 cubic feet per second of water into the stream channel and is classified as a rheocrene spring. Geology in the area is characterized by Mesozoic sedimentary rocks that have sandstone and limestone aquifer systems. The San Rafael Fault Zone is a northeast trending fault zone west of Acoma, and rocks have been down-dropped towards the east. Along the fault, the San Andres Limestone and Glorieta Sandstone (Psg), which forms a combined aquifer system, are just below alluvial cover and lava flows west of the fault; east of the fault the aquifer is displaced over 800 feet deeper below ground surface. The groundwater in the Psg, which flows from west to east, is brought to the surface due to juxtaposition of the Psg against the lower permeability Chinle Formation along the fault contact. This water discharges at a spring, Ojo del Gallo, and also recharges the alluvial-basalt aquifer. Horace Springs discharges from the alluvial-basalt aquifer downgradient (east) of the fault. Water chemistry was used to evaluate potential aquifers contributing to Horace Springs. Water that discharges at Horace Spring is predominantly derived from the Psg, with components from aquifers in the alluvial-basalt, Entrada Sandstone and Dakota Sandstone. 397
霍勒斯泉是在阿科马，新墨西哥州的普韦布洛的里约圣何塞常年到达的起点。由于蜿蜒的圣何塞河流经北部Horace Mesa和南部La Ventana Mesa之间的间隙，冲积含水层系统位于间隙中，导致冲积含水层横截面积减少，导致地下水排放到河床。目前，霍勒斯泉每秒向河道中排放约3.5至4立方英尺的水，被归类为异丙烯泉。该区地质特征为中生代沉积岩，具有砂岩和灰岩含水层系统。圣拉斐尔断裂带是阿科马以西的一个东北走向的断裂带，岩石向东下坠。沿着断层，圣安德烈斯石灰岩和格洛列塔砂岩(Psg)形成了一个联合含水层系统，就在断层西部的冲积盖层和熔岩流之下;断层东部的含水层被转移到地表以下800多英尺的地方。Psg中的地下水由西向东流动，由于Psg与低渗透率的Chinle组沿断层接触并置而被带到地表。这些水从一个叫Ojo del Gallo的泉水中流出，并重新注入冲积玄武岩含水层。贺拉斯泉从冲积玄武岩含水层向下(东)的断层流出。水化学被用来评价对贺拉斯泉有贡献的潜在含水层。从贺拉斯泉流出的水主要来自Psg，其成分来自冲积玄武岩、恩特拉达砂岩和达科他砂岩的含水层
{"title":"Hydrogeology and geochemistry of Horace Springs, Pueblo of Acoma, New Mexico","authors":"Christopher P. Wolf","doi":"10.56577/ffc-.397","DOIUrl":"https://doi.org/10.56577/ffc-.397","url":null,"abstract":"Horace Springs is the start of a perennial reach of the Rio San Jose at the Pueblo of Acoma, New Mexico. As the meandering Rio San Jose flows through a gap between Horace Mesa to the north and La Ventana Mesa to the south, the alluvial aquifer system lies in the gap, causing a decrease in the alluvial aquifer’s cross-sectional area resulting in groundwater discharging to the streambed. Horace Springs, currently, discharges about 3.5 to 4 cubic feet per second of water into the stream channel and is classified as a rheocrene spring. Geology in the area is characterized by Mesozoic sedimentary rocks that have sandstone and limestone aquifer systems. The San Rafael Fault Zone is a northeast trending fault zone west of Acoma, and rocks have been down-dropped towards the east. Along the fault, the San Andres Limestone and Glorieta Sandstone (Psg), which forms a combined aquifer system, are just below alluvial cover and lava flows west of the fault; east of the fault the aquifer is displaced over 800 feet deeper below ground surface. The groundwater in the Psg, which flows from west to east, is brought to the surface due to juxtaposition of the Psg against the lower permeability Chinle Formation along the fault contact. This water discharges at a spring, Ojo del Gallo, and also recharges the alluvial-basalt aquifer. Horace Springs discharges from the alluvial-basalt aquifer downgradient (east) of the fault. Water chemistry was used to evaluate potential aquifers contributing to Horace Springs. Water that discharges at Horace Spring is predominantly derived from the Psg, with components from aquifers in the alluvial-basalt, Entrada Sandstone and Dakota Sandstone. 397","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"40 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"123802331","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
From the mid-1800s to around 1930, monsoonal floods incised an arroyo roughly 100 m wide and 10 m deep along the lower Rio Puerco, NM, from the confluence with the Rio San Jose downstream to the mouth at the Rio Grande, causing sedimentation and flooding downstream. Since the 1930s, the channel has greatly narrowed, a densely vegetated floodplain has developed, the arroyo has partly filled, and downstream sedimentation has greatly decreased. Application of herbicide to a 12-km reach of the arroyo in 2003 to control non-native saltcedar (Tamarix spp.) prompted ongoing studies of channel change in the presence and absence of dense, riparian, woody vegetation. We used digital terrain models and satellite imagery to quantify changes in channel width and location in the sprayed reach and in an unsprayed reach downstream during a moderately low-flow interval (November 2006 to March 2010) and during an interval with a large flood (March 2010 to January/February 2014). Channel width increased in magnitude and variability in the sprayed reach but not in the unsprayed reach over both intervals, continuing a pattern first observed in an earlier study of the period 2003 to 2006. Since the herbicide application in 2003, there have been a total of five meander cutoffs in the sprayed reach and none in the unsprayed reach. In kilometer-long sections of the sprayed reach, channel width is now approaching that at the beginning of the period of channel narrowing in 1935. 439
{"title":"Contributions of moderately low flows and large floods to geomorphic change in the Rio Puerco Arroyo, New Mexico","authors":"E. R. Griffin, J. Friedman","doi":"10.56577/ffc-.439","DOIUrl":"https://doi.org/10.56577/ffc-.439","url":null,"abstract":"From the mid-1800s to around 1930, monsoonal floods incised an arroyo roughly 100 m wide and 10 m deep along the lower Rio Puerco, NM, from the confluence with the Rio San Jose downstream to the mouth at the Rio Grande, causing sedimentation and flooding downstream. Since the 1930s, the channel has greatly narrowed, a densely vegetated floodplain has developed, the arroyo has partly filled, and downstream sedimentation has greatly decreased. Application of herbicide to a 12-km reach of the arroyo in 2003 to control non-native saltcedar (Tamarix spp.) prompted ongoing studies of channel change in the presence and absence of dense, riparian, woody vegetation. We used digital terrain models and satellite imagery to quantify changes in channel width and location in the sprayed reach and in an unsprayed reach downstream during a moderately low-flow interval (November 2006 to March 2010) and during an interval with a large flood (March 2010 to January/February 2014). Channel width increased in magnitude and variability in the sprayed reach but not in the unsprayed reach over both intervals, continuing a pattern first observed in an earlier study of the period 2003 to 2006. Since the herbicide application in 2003, there have been a total of five meander cutoffs in the sprayed reach and none in the unsprayed reach. In kilometer-long sections of the sprayed reach, channel width is now approaching that at the beginning of the period of channel narrowing in 1935. 439","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"38 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"132049841","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Approximately 6 km east of the mouth of Abo Arroyo on the active floodplain of the Rio Grande, New Mexico, a 400-m exposure in the arroyo wall shows five preserved bluffs with buttress unconformities between Abo Arroyo and ancestral Rio Grande-derived sediments. The sources of sediments are identified by sediment color, clast types and bedding fabric. Ancestral Rio Grande sediments are pale, moderately well-sorted, and, where exposed, have basal straths immediately overlain by very well-rounded quartzite-bearing gravels and cobbles. Abo Arroyo sediments are red, show east-to-west inclined bedding in some places, are poorly sorted, and, in coarse facies, have subangular clasts from the catchment area. The oldest sediments, which Bluff 1 cross-cuts, are approximately 2.2 Ma, and the most recent sediments, younger than Bluff 5, have been deposited in the last century. The depositional history between Bluff 1 and Bluff 5 is difficult to interpret because of lack of age control, but cross-cutting relationships indicate the following. The oldest sediments in Bluff 1 were deposited during the aggrading period of the ancestral Rio Grande that ended at 800 ka. During the following 800 ky, the ancestral Rio Grande cut Bluffs 1-4. After cutting each bluff, the ancestral Rio Grande aggraded slightly and deposited floodplain sediments. The floodplain and distal Abo Arroyo fan deposits are interbedded, and grade upward into coarser Abo Arroyo pebbly sands. Bluff 1 was not exposed long enough to develop a wedge of colluvium before being buried. Bluffs 2 and 3 were buried by colluvium. Between Bluffs 2 and 3, it appears that there are continuous ancestral Rio Grande floodplain deposits, Abo Arroyo muds and steepening-upward fan deposits. Bluff 3 formed west of an older natural levee. Bluff 4 does not have colluvium and was rapidly buried by Abo Arroyo deposits. Bluff 5 was formed during recent (historical) incision by Abo Arroyo. This sequence shows the complex stratigraphic heterogeneity along the margin of axial river systems. It is difficult, if not impossible, to predict the subsurface depth to good aquifers in these sediments, given the intercalation of marginal tributary fans and streams with axial river bluff lines. 429
{"title":"Architecture of buried bluff lines: A record of the incising ancestral Rio Grande and Abo Arroyo from the Pleistocene to historical times","authors":"A. Rinehart, D. Love","doi":"10.56577/ffc-.429","DOIUrl":"https://doi.org/10.56577/ffc-.429","url":null,"abstract":"Approximately 6 km east of the mouth of Abo Arroyo on the active floodplain of the Rio Grande, New Mexico, a 400-m exposure in the arroyo wall shows five preserved bluffs with buttress unconformities between Abo Arroyo and ancestral Rio Grande-derived sediments. The sources of sediments are identified by sediment color, clast types and bedding fabric. Ancestral Rio Grande sediments are pale, moderately well-sorted, and, where exposed, have basal straths immediately overlain by very well-rounded quartzite-bearing gravels and cobbles. Abo Arroyo sediments are red, show east-to-west inclined bedding in some places, are poorly sorted, and, in coarse facies, have subangular clasts from the catchment area. The oldest sediments, which Bluff 1 cross-cuts, are approximately 2.2 Ma, and the most recent sediments, younger than Bluff 5, have been deposited in the last century. The depositional history between Bluff 1 and Bluff 5 is difficult to interpret because of lack of age control, but cross-cutting relationships indicate the following. The oldest sediments in Bluff 1 were deposited during the aggrading period of the ancestral Rio Grande that ended at 800 ka. During the following 800 ky, the ancestral Rio Grande cut Bluffs 1-4. After cutting each bluff, the ancestral Rio Grande aggraded slightly and deposited floodplain sediments. The floodplain and distal Abo Arroyo fan deposits are interbedded, and grade upward into coarser Abo Arroyo pebbly sands. Bluff 1 was not exposed long enough to develop a wedge of colluvium before being buried. Bluffs 2 and 3 were buried by colluvium. Between Bluffs 2 and 3, it appears that there are continuous ancestral Rio Grande floodplain deposits, Abo Arroyo muds and steepening-upward fan deposits. Bluff 3 formed west of an older natural levee. Bluff 4 does not have colluvium and was rapidly buried by Abo Arroyo deposits. Bluff 5 was formed during recent (historical) incision by Abo Arroyo. This sequence shows the complex stratigraphic heterogeneity along the margin of axial river systems. It is difficult, if not impossible, to predict the subsurface depth to good aquifers in these sediments, given the intercalation of marginal tributary fans and streams with axial river bluff lines. 429","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"31 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"114388709","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
{"title":"A geologic summary of the Llano de Albuquerque: A diachronous ~1.5-1.65 (?) Ma geomorphic surface complex marking the cessation of Santa Fe Group deposition in the western Albuquerque Basin","authors":"D. Mccraw","doi":"10.56577/ffc-.83","DOIUrl":"https://doi.org/10.56577/ffc-.83","url":null,"abstract":"","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"44 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"128871783","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
{"title":"An overview of Hidden Mountain: Geology, archaeology, and the mystery stone","authors":"D. Mccraw","doi":"10.56577/ffc-.112","DOIUrl":"https://doi.org/10.56577/ffc-.112","url":null,"abstract":"","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"1 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"121364584","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Although the geochemistry of the mineralized waters from springs on the eastern flank of the Lucero uplift has been the subject of several geothermal investigations, measured temperatures in oil and water wells in the uplift and adjacent Acoma basin have received little attention. Bottom hole temperature (BHT) measurements in oil wells and discharge temperatures from water wells reveal three structural zones that warrant further investigation. BHTs in two oil wells on the west flank of the Lucero uplift in the Correo fault zone have elevated temperatures of 65 to 71°C at a depth of ca. 1100 m. These wells are located ca. 7 km northeast of the youthful (>192 ka) Lucero volcanic field. Two distinct bands of water wells located near the Hickman and Red Lake fault zones on margins of the Acoma basin that tap the San Andres-Glorieta aquifer have elevated discharge temperatures of 34 to 52.8°C (depths 615 to 884 m). We also apply a novel analysis of conservative ion (boron and lithium) data using reverse particle-tracking (upwinding) to locate the source of high concentration plumes along the east side of the Lucero uplift and within the Acoma basin. Wells with highest temperatures and conservative ion concentrations are found on the down gradient end of a gravity driven flow system. The <80°C geothermal resource in this area could be used for greenhouses and similar low-temperature applications. 263
{"title":"Low-temperature geothermal resources in the Acoma Basin and Lucero Uplift, eastern Cibola and western Valencia counties, New Mexico","authors":"S. Kelley, M. Person, R. Kelley, J. Pepin","doi":"10.56577/ffc-.263","DOIUrl":"https://doi.org/10.56577/ffc-.263","url":null,"abstract":"Although the geochemistry of the mineralized waters from springs on the eastern flank of the Lucero uplift has been the subject of several geothermal investigations, measured temperatures in oil and water wells in the uplift and adjacent Acoma basin have received little attention. Bottom hole temperature (BHT) measurements in oil wells and discharge temperatures from water wells reveal three structural zones that warrant further investigation. BHTs in two oil wells on the west flank of the Lucero uplift in the Correo fault zone have elevated temperatures of 65 to 71°C at a depth of ca. 1100 m. These wells are located ca. 7 km northeast of the youthful (>192 ka) Lucero volcanic field. Two distinct bands of water wells located near the Hickman and Red Lake fault zones on margins of the Acoma basin that tap the San Andres-Glorieta aquifer have elevated discharge temperatures of 34 to 52.8°C (depths 615 to 884 m). We also apply a novel analysis of conservative ion (boron and lithium) data using reverse particle-tracking (upwinding) to locate the source of high concentration plumes along the east side of the Lucero uplift and within the Acoma basin. Wells with highest temperatures and conservative ion concentrations are found on the down gradient end of a gravity driven flow system. The <80°C geothermal resource in this area could be used for greenhouses and similar low-temperature applications. 263","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"431 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"124235583","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Between November 1989 and June 1991, a strong earthquake swarm near Bernardo, New Mexico occurred within the Rio Grande rift. Using data from their short-period seismograph network, temporarily deployed seismic stations, and other regional seismic data, researchers at New Mexico Tech observed four earthquakes of between duration magnitude 4.1 and 4.7 (all felt in Socorro), and many additional smaller earthquakes. The Gutenberg-Richter relationship between earthquake frequency and magnitude for the swarm has a b-value of 0.57, or fewer small events relative to the numbers of large events than is typically observed for tectonic areas (where b-values are close to 1). The best-constrained aftershock locations following the two largest events cover epicentral areas of between 4 and 4.5 km2, with depths ranging between 4 and 6.5 km. Aftershock trends, focal mechanism solutions from first motions, and modeling of regional broadband data conducted by other researchers suggest the swarm occurred along adjacent, nearly parallel normal faults with strikes trending slightly east of north. The events occurred just above a west-to-east trending listric fault previously imaged on active-source crustal profiles obtained in the Bernardo area. Thus, a triggering mechanism for the Bernardo swarm may be aseismic movement on the east-trending listric fault stressing north-trending normal faults in the shallower crust above. 225
{"title":"Anatomy of a strong and prolonged Rio Grande Rift earthquake swarm","authors":"A. Sanford, H. Hartse","doi":"10.56577/ffc-.225","DOIUrl":"https://doi.org/10.56577/ffc-.225","url":null,"abstract":"Between November 1989 and June 1991, a strong earthquake swarm near Bernardo, New Mexico occurred within the Rio Grande rift. Using data from their short-period seismograph network, temporarily deployed seismic stations, and other regional seismic data, researchers at New Mexico Tech observed four earthquakes of between duration magnitude 4.1 and 4.7 (all felt in Socorro), and many additional smaller earthquakes. The Gutenberg-Richter relationship between earthquake frequency and magnitude for the swarm has a b-value of 0.57, or fewer small events relative to the numbers of large events than is typically observed for tectonic areas (where b-values are close to 1). The best-constrained aftershock locations following the two largest events cover epicentral areas of between 4 and 4.5 km2, with depths ranging between 4 and 6.5 km. Aftershock trends, focal mechanism solutions from first motions, and modeling of regional broadband data conducted by other researchers suggest the swarm occurred along adjacent, nearly parallel normal faults with strikes trending slightly east of north. The events occurred just above a west-to-east trending listric fault previously imaged on active-source crustal profiles obtained in the Bernardo area. Thus, a triggering mechanism for the Bernardo swarm may be aseismic movement on the east-trending listric fault stressing north-trending normal faults in the shallower crust above. 225","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"21 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"129008341","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
{"title":"The historical Belen Harvey House and Museum","authors":"Jamie Petersen","doi":"10.56577/ffc-.90","DOIUrl":"https://doi.org/10.56577/ffc-.90","url":null,"abstract":"","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"50 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"124124601","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
{"title":"Chinle Group (upper Triassic) limestone at Carrizo Spring, Valencia county, New Mexico","authors":"S. Lucas, L. Tanner","doi":"10.56577/ffc-.114","DOIUrl":"https://doi.org/10.56577/ffc-.114","url":null,"abstract":"","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"39 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"126815274","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
Red beds of the Early Permian Abo Formation and overlying DeChelly Sandstone (Yeso Group) in the Lucero uplift of central New Mexico are locally rich in fossil tetrapod footprints. The New Mexico Museum of Natural History and Science in Albuquerque, New Mexico, houses 30 specimens with tetrapod footprints from 18 different localities within the study area. The assemblage includes tracks of Amphisauropus Haubold, 1970, Ichniotherium Pohlig, 1892, Hyloidichnus Gilmore, 1927, and Dromopus Marsh, 1894, that are referred to seymouriamorph, diadectomorph, captorhinid and parareptile or diapsid eureptile trackmakers. The relative abundance of Amphisauropus tracks seems to be a characteristic feature of Early Permian tetrapod footprint assemblages in central New Mexico that are intermediate between coastal plain and inland to upland paleoenvironments. Based on vertebrate tracks, the upper part of the Abo Formation in the study area is suggested to be of late Early Permian (~Artinskian/late Wolfcampian to early Leonardian) age. 387
{"title":"Permian tetrapod footprints from the Lucero Uplift, central New Mexico","authors":"S. Voigt, S. Lucas","doi":"10.56577/ffc-.387","DOIUrl":"https://doi.org/10.56577/ffc-.387","url":null,"abstract":"Red beds of the Early Permian Abo Formation and overlying DeChelly Sandstone (Yeso Group) in the Lucero uplift of central New Mexico are locally rich in fossil tetrapod footprints. The New Mexico Museum of Natural History and Science in Albuquerque, New Mexico, houses 30 specimens with tetrapod footprints from 18 different localities within the study area. The assemblage includes tracks of Amphisauropus Haubold, 1970, Ichniotherium Pohlig, 1892, Hyloidichnus Gilmore, 1927, and Dromopus Marsh, 1894, that are referred to seymouriamorph, diadectomorph, captorhinid and parareptile or diapsid eureptile trackmakers. The relative abundance of Amphisauropus tracks seems to be a characteristic feature of Early Permian tetrapod footprint assemblages in central New Mexico that are intermediate between coastal plain and inland to upland paleoenvironments. Based on vertebrate tracks, the upper part of the Abo Formation in the study area is suggested to be of late Early Permian (~Artinskian/late Wolfcampian to early Leonardian) age. 387","PeriodicalId":243410,"journal":{"name":"Guidebook 67 - Geology of the Belen Area","volume":"18 1","pages":"0"},"PeriodicalIF":0.0,"publicationDate":"1900-01-01","publicationTypes":"Journal Article","fieldsOfStudy":null,"isOpenAccess":false,"openAccessPdf":"","citationCount":null,"resultStr":null,"platform":"Semanticscholar","paperid":"125857932","PeriodicalName":null,"FirstCategoryId":null,"ListUrlMain":null,"RegionNum":0,"RegionCategory":"","ArticlePicture":[],"TitleCN":null,"AbstractTextCN":null,"PMCID":"","EPubDate":null,"PubModel":null,"JCR":null,"JCRName":null,"Score":null,"Total":0}
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