Ash-flow tuffs and cauldrons in the northeast Mogollon-Datil volcanic field--A summary

Osburn, Glenn R.; Chapin, Charles E.

doi:10.56577/ffc-34.197

Cited by 14 publications

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“…The block is made up of Proterozoic granite overlain by a thick (approximately 2100 to 2400 m) section of Pennsylvanian to Cretaceous sedimentary rocks and Cenozoic volcanic and sedimentary units. The youngest ash flow tuff that covers this area has an 40Ar/39Ar age of 27.36 ± 0.07 Ma (McIntosh et al, 1990;Osburn and Chapin, 1983). The block is bounded on the east by the enigmatic East Joyita fault, which separates Proterozoic rocks on the west from Cenozoic volcanic rocks on the east.…”

Section: Central New Mexicomentioning

confidence: 97%

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Late Mesozoic to Cenozoic cooling histories of the flanks of the northern and central Rio Grande rift, Colorado and New Mexico

Kelley¹,

Chapin²,

Corrigan³

1992

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Apatite fission-track (FT) data collected in the northern and central Rio Grande rift of NM and CO indicate that rocks now exposed in the eastern and western margins of the rift cooled during uplift and erosion in a complex spatial and temporal pattern. FT data from the Santa Fe Range, Los Pinos Mountains, and northern Nacimiento Mountains indicate that these mountain blocks cooled during the early stage of the Laramide orogenic event. Other mountain blocks began cooling during the late stage of the Laramide event and subsequent Eocene erosion. The Sandia Mountains, Blanca Peak, Joyita Hills, Sierra Ladrones, the high-elevation portion of the Sawatch Range, and the lower-elevation samples in the Sangre de Cristo Mountains began cooling during early extension of the Rio Grande rift and/or waning of regional volcanism in the late Oligocene and early Miocene. The eastern front of the Sawatch Range, the Sangre de Cristo Mountains north of Blanca Peak, the low-elevation portion of the Sangre de Cristo Mountains near San Luis, Colorado, and the Lemitar Mountains cooled during late-stage rifting in middle to late Miocene. Generally, the youngest FT ages are found in the rift flanks adjacent to large normal faults along the deep margins of the en echelon half-grabens that make up the present Rio Grande rift. Two of the blocks with Miocene FT ages, the Sierra Ladrones and Blanca Peak, are promontories that project into the rift basins at the junction of arcuate normal faults bounding the deep side half-grabens. Tectonic denudation of three sides has allowed unusually rapid isostatic uplift in these blocks. Similarly, the Sangre de Cristo Mountains north of Blanca Peak are bounded on two sides by active late Cenozoic faults that have allowed the rapid isostatic rise of these mountains. Cooling rates increased from the Laramide orogenic event (1 deg. to 4 deg. C/Ma) to the development of the Rio Grande rift (7 deg. to 20 deg. C/Ma).The Southern Rocky Mountains in CO and NM have had a long and complex geologic history, culminating in the Late Cretaceous to late Eocene with the compressional Laramide orogenic event. A widespread surface of low relief was carved across much of the area in late Eocene. Major volcanism affected the province during the Oligocene. The Rio Grande rift, an extensional feature that bisects the Southern Rocky Mountains, began to form about 30 Ma and developed during two phases of regional extension. The early northeast-southwest-oriented phase of extension is characterized by the development of broad, shallow basins, low-amplitude topographic relief, local areas of intense extensions associated with low-angle normal faults, and the emplacement of large volumes of silicic ash-flow tuffs and basaltic andesite lavas. The later phase of extension is characterized by the development of deep half-grabens, high topographic relief, the formation of widely spaced, high-angle normal faults, and the emplacement of alkali-olivine and tholeiitic basalts.The tectonic development of Southern Rocky Mountains in the vicinity of the rift has been determined primarily by studying the depositional and structural history of sedimentary and volcanic rocks preserved in and adjacent to the rift basins. Two of the basins of the northern Rio Grande rift, the San Luis Basin and the Albuquerque-Belen Basin, are largely undissected so that the early history in these basins is not well constrained, although data from seismic lines and petroleum test wells have improved the understanding of these areas in recent years. Little has been done to estimate the uplift rate or timing of uplift of the mountain ranges that bound the margins of the rift. Many of the rift models in the literature predict uplift rates, but there are few data to test these predictions. Fission-track data from rocks exposed along the flanks of the rift provide powerful constraints for these models.

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Section: Central New Mexicomentioning

confidence: 97%

“…Magdalena Mountains-The Magdalena Mountains (Fig. 16) consist primarily of 20 to 40 Ma volcanic rocks that were generally erupted from several overlapping, nested cauldrons (Chapin et al, 1978;Osburn and Chapin, 1983). The volcanic rocks overlie Proterozoic crystalline rocks and Paleozoic sedimentary rocks.…”

Section: Central New Mexicomentioning

confidence: 99%

Late Mesozoic to Cenozoic cooling histories of the flanks of the northern and central Rio Grande rift, Colorado and New Mexico

Kelley¹,

Chapin²,

Corrigan³

1992

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“…The Palm Park Formation was named by Kelley and Silver (1952) for exposures in Palm Park, located adjacent to Red House Mountain in the southern part of the Caballo Mountains. Mapped extensively throughout south-central New Mexico, the formation has also been correlated with the Rubio Peak Formation in the Silver City region (Elston, 1957), the Spears Formation in the Socorro-Datil region (Tonking, 1957;Osburn and Chapin, 1983), and with the Orejon Andesite and Cleofas Andesite of the Las Cruces area (Dunham, 1935;Seager et al, 1976;Seager, 1981). In the Caballo Mountains, the formation crops out widely in Apache Valley and in the McLeod syncline, as well as in Palm Park.…”

Section: Palm Park Formationmentioning

confidence: 93%

Geology of the Caballo Mountains, New Mexico

Seager¹,

Mack²

2003

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The Caballo Mountains, just south of Truth or Consequences, rise to an elevation of 7,065 feet. Today they are flanked on the west side by Caballo Reservoir and on the east side by the Jornada del Muerto. An extraordinary geologic section is preserved here. Precambrian igneous and metamorphic rocks (granites and schists) provide a view of the Precambrian history of this part of the country, and an extraordinary thickness of sedimentary rocks (whose collective thickness is more than 3.5 miles) gives us an unparalleled picture of the evolution of southern New Mexico. Development of these mountains began with compression and uplift associated with the Laramide orogeny, at the end of the Mesozoic. Since then the complex geologic history of this part of New Mexico has included uplift, erosion, faulting, volcanic activity, continental deposition, and, finally, the development of the Rio Grande rift. That complex geologic history is well documented in this volume. This memoir is the result of many years of study and field work on the part of the authors, who have drawn together in one place this comprehensive description of the region. The volume is heavily illustrated with photographs, maps, stratigraphic sections, and other graphics. It contains both an index and a glossary.

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“…Based on the relatively high quartz and volcanic-lithic percentages, the pre-Santa Fe Tertiary section in the wells is believed to correlate mainly with the unit of Isleta #2 well of Lozinsky (1988). This informal unit is at least partly equivalent to the Datil Group and probably includes portions of the sequence from Hells Mesa Tuff through South Canyon Tuff and La Jara Peak Basaltic Andesite that overlie the Datil Group as defined by Osburn and Chapin (1983). Because this unit may include the overlying sequence of volcanic units in addition to the Datil Group, it was given its own informal name for convenience.…”

Section: Pre-santa Fe Tertiary Depositsmentioning

confidence: 99%

Geology and paleontology of the Santa Fe Group, southwestern Albuquerque Basin, Valencia County, New Mexico

Lozinsky¹,

Tedford²

1991

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Santa Fe Group outcrops in the southwestern Albuquerque Basin occur in the Gabaldon badlands and Bobo Butte areas. Two oil test wells located near the Gabaldon badlands, the Humble Santa Fe Pacific #1 and Shell Santa Fe Pacific #2, penetrate the Santa Fe Group and pre-Santa Fe Tertiary deposits and bottom in Mesozoic bedrock.In the Gabaldon badlands, the thickness of the exposed Santa Fe Group is at least 1,138 m (3,732 ft) and may be as much as 1,800 m (6,000 ft). In the Humble Santa Fe Pacific #1 and Shell Santa Fe Pacific #2 wells, the Santa Fe thickness is 1,494 and 1,460 m (4,902 and 4,790 ft), respectively. The thickness of the exposed Santa Fe section at Bobo Butte is 246 m (807 ft). In the oil test wells, up to 1,097 m (3,600 ft) of pre-Santa Fe Group Tertiary deposits, which are correlative with possible Baca Formation and an unnamed post-Baca/pre-Santa Fe unit, underlie the Santa Fe Group. These pre--Santa Fe deposits indicate the presence of a depositional basin that predates the Albuquerque Basin.The Santa Fe Group exposed in the Gabaldon badlands area is divided into four units that correlate with the Popotosa Formation (units 1-3) and the Sierra Ladrones Formation. Units 1-3 of the Popotosa Formation were deposited in a closed-basin, distal-fan/basin-floor environment at a calculated sedimentation rate of 204 m/m.y. (669 ft/m.y.). The Sierra Ladrones Formation was deposited by a large, throughflowing, fluvial system and local alluvial-fan distributaries on adjacent piedmont slopes. Santa Fe Group deposits in the Bobo Butte area correlate with parts of the Popotosa Formation and were deposited in a proximal fan area. The caprock unit on Bobo Butte is probably correlative with at least part of the Sierra Ladrones Formation.Analysis of outcrop and thin-section data indicates that the Popotosa Formation in the southwestern Albuquerque Basin was derived from the Lucero uplift. At the time units 1-3 were deposited, the Lucero uplift was covered by at least one Tertiary ash-flow-tuff sheet and Upper Cretaceous strata. These rocks have since been eroded from the Lucero uplift and deposited in the southwestern Albuquerque Basin. The fluvial facies of the Sierra Ladrones Formation was at least partly derived from more distant source areas to the west and northwest. Outcrop data show that the caprock unit on Bobo Butte was derived from the Lucero uplift.Vertebrate fossils recovered from the Gabaldon badlands include Epicyon sp. cf. E. haydeni validus, Dipoides sp. cf. D. vallicula, Michenia sp. cf. M. yavapaiensis, and Plioceros sp. Fossils from units 2 and 3 indicate an early Hemphillian age (7-9 Ma), and the upper part of unit 1 is perhaps slightly older (latest Clarendonian).

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Ash-flow tuffs and cauldrons in the northeast Mogollon-Datil volcanic field--A summary

Cited by 14 publications

References 0 publications

Late Mesozoic to Cenozoic cooling histories of the flanks of the northern and central Rio Grande rift, Colorado and New Mexico

Late Mesozoic to Cenozoic cooling histories of the flanks of the northern and central Rio Grande rift, Colorado and New Mexico

Geology of the Caballo Mountains, New Mexico

Geology and paleontology of the Santa Fe Group, southwestern Albuquerque Basin, Valencia County, New Mexico

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