The nautiloid order Ellesmeroceratida

Flower, Rousseau H.

doi:10.58799/m-12

Cited by 12 publications

(40 citation statements)

References 9 publications

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“…Elston (1958) and Turner (1962) discussed the position of the Florida Mountains relative to the Burro uplift and Deming axis. Discussions on relations of rocks in the Florida Mountains to surrounding areas also are included in Armstrong and Mamet (1978), Bogart (1953), Darton (1917aDarton ( , 1928, Flower (1953aFlower ( , b, 1958Flower ( , 1964Flower ( , 1965Flower ( , 1969, Greenwood et al (1970), Hawley (1981), Hayes (1970Hayes ( , 1975a, Howe (1959), Jicha (1954), Kelley and Bogart (1952), Kelley and Silver (1952), Kottlowski (1957Kottlowski ( , 1958bKottlowski ( , 1960Kottlowski ( , 1962Kottlowski ( , 1963Kottlowski ( , 1965aKottlowski ( , b, 1971aKottlowski ( , b, 1973, Kottlowski and Foster (1962), Kottlowski and Pray (1967), Kottlowski, Foster, and Wengerd (1969), Kottlowski, LeMone, and Foster (1969), Lemley (1982), LeMone (1969aLeMone ( , b, c, 1974LeMone ( , 1976a, Lochman-Balk 0958, 1974), Loring and Armstrong (1980), Lucia (1969), Lynn (1975), Thompson (1982), Thompson and ...…”

Section: Previous Workmentioning

confidence: 99%

“…Kelley and Silver (1952) raised the El Paso to group statu s, with Sierrite (below) and Bat Cave (above) Formations. Flower (1958Flower ( , 1964Flower ( , 1969 and LeMone (1969a, b, c) adopted the group status and assigned formational names to about 10 faunal zones and lithologic units. Lucia (1969) regarded the El Paso as a group and divided it into six formations.…”

Section: El Paso Formationmentioning

confidence: 99%

“…The allochems are listed in order of decreasing abundance, and a trace is considered to be less than 1 % of the total allochems. Flower (1964Flower ( , 1969 and LeMone (1969a). The section was measured using a Jacob's staff and Brunton compass.…”

Section: Appendix A-2mentioning

confidence: 99%

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Geology of the Florida Mountains, southwestern New Mexico

Clemons¹

1998

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The Florida Mountains are an eastward-tilted Basin and Range fault block approximately 24 km (15 mi) southeast of Deming. The mountains are surrounded by a broad bajada that slopes gently into the Mimbres Basin. Sediments conceal the range-bounding faults except at the northwest end. Ephemeral streams are continuing the erosive processes that have reduced the exposed bedrock area to less than one-half of its initial size.The oldest rocks exposed in the Florida Mountains are Precambrian hornblende and granitic gneisses exposed only north of Capitol Dome. An Upper Cambrian pluton intruded an andesitic to basaltic volcanic sequence producing the hornblende and pyroxene hornfels common in the western and southern parts of the mountains. The alkali-feldspar plutonic rocks are granite at the northern and southern ends of the range and syenite and quartz syenite in the central part. These shallow plutonic rocks and hornfels were unroofed before deposition of a diamictite that, in turn, was mostly eroded preceding deposition of the Bliss Sandstone in Early Ordovician time. Approximately 4,100 ft of Paleozoic rocks that crop out in the southeastern Florida Mountains include, in ascending order: Bliss Sandstone, El Paso Formation, Montoya Formation, Fusselman Dolomite, Percha Shale, Rancheria Formation, and Hueco Formation. No Mesozoic rocks are present except possibly the basal beds of the Lobo Formation, the bulk of which was deposited penecontemporaneously with Laramide deformation during Paleocene and early to middle Eocene times. Extensive andesitic to rhyolitic volcanism from middle Eocene to early Miocene times accounted for the thick Rubio Peak volcaniclastic section forming Florida Peak, as well as the ash-flow tuff, air-fall tuffs, flow-banded rhyolite, basaltic andesite, and dacite in the Little Florida Mountains. Thick rhyolite fanglomerates in the Little Florida Mountains and alluvial conglomerates forming an apron around the mountains have been deposited as the mountain block was uplifted approximately 213 m (7,000 ft) since early Miocene.The south Florida Mountains fault is a northwest-trending, high-angle reverse fault that places Upper Cambrian granite against rocks as young as basal Lobo Formation. Multiple, small thrust faults exhibit younger-over-older rocks relations and produce tectonic elimination of strata. A few show older-over-younger relations. Current studies demonstrate that Laramide deformation in the Florida Mountains is not a continuation of the Cordilleran overthrust belt. Evidence suggests that the deformation resembles the basement-cored uplifts of the Rocky Mountain foreland, with possibly some strike-slip components.Hydrothermal alteration and low-grade mineralization are widespread in the Florida and Little Florida Mountains. Relatively limited activity has produced manganese, zinc, lead, silver, copper, barite, and fluorite ores. Most production of copper, zinc, lead, and silver ores was from shallow oxidized veins, but small amounts of chalcopyrite accompany fluorite and barite in deeper veins. The age of mineralization is believed to be late Tertiary. Although the mountains had been mapped before (by Darton in 1916 and by Corbitt in 1971), questions about interpretations of several aspects of the geology of the Florida Mountains had not been settled: Are the plutonic rocks of Precambrian, Ordovician, Mesozoic, or some other age? Are the plutonic rocks related, or were they formed by multiple episodes of plutonism? Are the gabbros and diorites (hornfelses) older or younger than the granites and syenites? What is the origin of the south Florida Mountains fault and associated thrust faults? Are they part of the Cordilleran overthrust belt? Clemons spent nearly two decades mapping in the Florida Mountains trying to answer these (and other) questions.Rather than hold all the data until completion of mapping and laboratory studies, several progress reports and four geologic maps (GM-52, Geology of Florida Gap quadrangle, 1982; GM-58, Geology of Gym Peak quadrangle, 1983; GM-56, Geology of Capitol Dome quadrangle, 1984; and GM-59, Geology of South Peak quadrangle, 1985) were published previously. Terminology, interpretation, and ideas in this report represent revisions from Clemons' earlier publications.

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Section: Previous Workmentioning

confidence: 99%

Section: El Paso Formationmentioning

confidence: 99%

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Geology of the Florida Mountains, southwestern New Mexico

Clemons¹

1998

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“…2). Flower (1958Flower ( , 1959 recognized distinct faunal zones in the El Paso Group and later applied geographic names to the faunal units (Flower, 1964), which then became known as formal formations (Fig. 2).…”

Section: Nomenclaturementioning

confidence: 99%

“…The Hitt Canyon was named by Hayes for its type section, described by Harbour (1972), on the east side of the northern Franklin Mountains. The Hitt Canyon is equivalent to unit A used by Cloud and Barnes (1948) and to five formations used by Flower (1964) in the Franklin Mountains. For the middle unit, Hayes used the name McKelligon, a formation named by Flower (1964) for a section at McKelligon Canyon in the southern Franklin Mountains that was later assigned by LeMone (1969) as a type section.…”

Section: Nomenclaturementioning

confidence: 99%

Petrography and depostional environments of the Lower Ordovician El Paso Formation

Clemons¹

1991

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The Lower Ordovician (Canadian) El Paso Formation conformably overlies Bliss Sandstone across most of southern New Mexico and west Texas. Locally, lower El Paso beds overlie plutonic and volcanic rocks. Field examination, sampling, and petrographic study of 38 stratigraphic sections from southeastern Arizona, across southern New Mexico, to Van Horn, Texas, indicate the El Paso was deposited in shallow waters near a shoreline to the north. The southwestern edge of the North American craton had subsided gradually throughout most of Canadian time, receiving the up-to 420-m-thick El Paso carbonate blanket.The El Paso Formation is subdivided by lithology into four members that are recognized throughout the region. In ascending order, the members are the Hitt Canyon (33-136 m), the Jose (3-33 m), the McKelligon (45-190 m), and the Padre (35-117 m). The gradually decreasing sand content upward through the Hitt Canyon Member indicates the Hitt Canyon was deposited farther from shore in waters that became deeper as the seas transgressed northward. Girvanella oncolites are locally abundant. Stromatolite mounds near the top of the Hitt Canyon and the presence of sand, ooids, and rounded bioclasts in the Jose Member record a shoaling environment. The McKelligon Member contains little or no sand; at several locales sponge-Calathium mounds and stromatolite mounds are prominent. The Padre contains a more restricted fauna that includes traces of ostracods. Beds in the lower part of the Padre Member are silty to sandy and locally contain thinly laminated zones.There is no correlation between stratigraphic members of the El Paso Formation and occurrences of dolostone. Beds in the lower part of the Hitt Canyon Member are typically dolostone, but are limestone at 25% of the sections studied. The El Paso Formation is mostly to completely dolostone at Beach Mountain near Van Horn, Texas, at Bishop Cap, and in the Sacramento, San Andres, Oscura, and Pedregosa Mountains. The El Paso is predominantly limestone at San Diego Mountain and in the Caballo and Mud Springs Mountains, 60 km west of the Bishop Cap-San Andres-Oscura Mountains trend. At other locales, the limestone/dolostone ratios vary with no apparent geographic relationship. Locally, single beds of dolostone are interbedded with limestone sections. More typically, dolostone or limestone prevails for tens of meters of section. Evidence of supratidal dolostone is lacking except in some beds in the Jose and Padre Members. Hydrothermal dolostone is common in several sections.Pervasive bioturbation of El Paso Formation beds and a varied biota of echinoderms, sponges, gastropods, trilobites, Nuia, Calathium, cephalopods, and algae (plus minor brachiopods, Pulchrilamina, and ostracods) indicate a predominantly shallow-subtidal environment. Intertidal conditions prevailed intermittently, and possibly supratidal deposition took place during parts of Jose and early Padre times. Low-energy platform environments, in which a large volume of micritic muds accumulated, were often disturbed by storms that produced abundant thin, poorly washed biosparite, intrasparite, and intrasparrudite (bioclastic and intraclastic grainstone) lenses.

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