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GeoRef Subject
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Primary terms
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Africa
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Solitario
ABSTRACT Upper Cambrian through Middle Ordovician sedimentary strata of the Marathon/Solitario Basin (west Texas), which were folded and thrust-faulted during late Paleozoic Appalachian-Ouachita orogenesis, preserve evidence of the pre-Pangean history of the central southern Laurentian margin. New detrital zircon analyses reported here are from three Marathon Basin/Solitario formations: the upper Cambrian Dagger Flat Sandstone; the Lower Ordovician Marathon Formation, including the Rodrigues Tank Sandstone Member; and the Middle Ordovician Ft. Peña Formation. The far-southwestern outcrops of those Iapetus margin strata are within the Solitario dome (Presidio and Brewster Counties, Texas). Solitario zircon U/Pb geochronological results (laser ablation–inductively coupled plasma–mass spectrometry [LA-ICP-MS], sensitive high-resolution ion microprobe [SHRIMP]) expand the record of Cryogenian rifting as the Cuyania terrane separated from Laurentia. We evaluated these new data along with earlier geochronological and geochemical results from rift-related lava clasts in Lower–Middle Ordovician sedimentary subaqueous debris-flow deposits in the northwestern Marathon Basin. Deepening of the Iapetus seaway near the Laurentian margin (late Cambrian–Middle Ordovician) stimulated headward erosion of drainages, reflected in the systematic north-northwestward shift in zircon provenance from the west Texas Grenvillian and Southern Granite-Rhyolite Provinces to Yavapai-Mazatzal and Cheyenne Belt sources. The Cuyania rifted terrane underwent subduction at the western Gondwanan margin of the Iapetus Ocean in mid-Ordovician time (486 ± 7 Ma to 463 ± 4 Ma), and the resulting volcanism in the Famatina complex (Argentina) was most intense from ca. 472 to 468 Ma. Magmatic zircons from Ft. Peña bentonitic layers have identical U/Pb (488–468 Ma) and biostratigraphic (Darriwilian) ages to those from Famatinian bentonites at Talacasto (470 ± 5 Ma) in the Precordillera of Cuyania. Geologically constrained paleomagnetic reconstructions for 470 Ma depict the proximity of the Famatina arc, the rifted Cuyania terrane, and southern Laurentia at low southern latitudes (equator to ~30°S). These first U/Pb geochronological data from the Marathon/Solitario depocenter of western Iapetus appear to be compatible with such a configuration and can serve as test data for emerging tectonic interpretations.
Igneous evolution of a complex laccolith-caldera, the Solitario, Trans-Pecos Texas: Implications for calderas and subjacent plutons
A Laramide age push-up block: The structures and formation of the Terlingua-Solitario structural block, Big Bend region, Texas: Discussion and reply
Geology of the Solitario, Trans-Pecos Texas (Geological Society of America Special Paper 250): Discussion and reply
A Laramide-age push-up block: The structures and formation of the Terlingua-Solitario structural block, Big Bend region, Texas
Geology of the Solitario, Trans-Pecos Texas
The Solitario displays geologic features that span virtually the entire regional history of Trans-Pecos Texas since Cambrian time. The visible structure (cover) is the eroded remnant of the roof of a radially symmetric late Eocene (38 Ma) laccolith. Erosion of the laccolith roof has exposed a remarkably complete stratigraphic section. The rock record begins with Upper Cambrian Dagger Flat Sandstone. Deposition of Upper Cambrian sand and shale in a shallow sea gave way during Ordovician to deposition of black shales interbedded with some sand and black chert, reflecting more restricted circulation. About 1 km of sediments, from the craton to the north and northwest, accumulated in the Ouachita Trough during Late Cambrian and Ordovician time. The area was elevated and slightly tilted, but not significantly deformed, by the Llanorian Orogeny during Silurian time. Silurian rocks are missing, and the Lower Devonian-Mississippian Caballos Novaculite rests unconformably on the Upper Ordovician Maravillas Formation. More than 1.4 km of flysch, from a source to the southeast, forms the Mississippian-Pennsylvanian Tesnus Formation. No Paleozoic rocks younger than Early Pennsylvanian (Morrowan Series) have been found. The measured thickness of Paleozoic rocks in the Solitario is approximately 2.6 km and represents a time span of 240 m.y., with a single break of ~30 m.y. during Silurian, one of the longest depositional records known. The Paleozoic rocks presently found in the Solitario are allochthonous and were intensely deformed during the Ouachita Orogeny. The orogeny affected the Solitario area from Middle Pennsylvanian (Desmoinesian) until Early Permian (middle Wolfcampian). Transport of the allochthon during the Ouachita Orogeny was at least tens of kilometers from the southeast. Deformation was primarily by folding, with the development of nappes, S-folds, boudinage structures, and local and regional thrust faults evident in the exposed Paleozoic rocks. After the Ouachita Orogeny, the Solitario area remained positive from Early Permian (middle Wolfcampian) on the structural block known as the Tascotal Uplift that formed the southern margin of the Permian sea. Throughout early Mesozoic, the area remained elevated on the West Texas-Coahuila Platform, and was extensively eroded as part of the Wichita paleoplain. In Early Cretaceous (late Aptian), the area was covered by a shallow sea, and 1.2 km of carbonates were deposited. These rocks are now magnificently exposed in cross section in the shutups that cut the rim of the Solitario dome. The Cretaceous rocks are correlative with carbonate units found to the east and south in the Gulf Coast area. At the end of the Cretaceous (Gulfian), the area was elevated once again as the Laramide Orogeny migrated eastward. Regionally, the Solitario lies on a large structural block that is defined by gravity data as a remnant of the Tascotal Uplift. The block appears to have responded to Laramide compression by uplift and rigid-body rotation without undergoing extensive internal deformation. Deformation associated with the Laramide Orogeny had no discernible effect on the later emplacement of the Solitario laccolith. Within the mapped area, Laramide compression is, at most, presently evident only as sparse stylolites in the Cretaceous rim rocks. Mid-Eocene basal conglomerate of the Devils Graveyard Formation, shed from Laramide folds to the west, is found in Fresno Canyon, and is the only Tertiary rock that predates the formation of the Solitario dome. The oldest reliably dated igneous rock in the Solitario is a 37.5 ± 0.8 Ma rhyolite sill. The sill intruded the base of the Cretaceous section immediately prior to the formation of the Solitario dome. The dome was formed by intrusion of ~100 km 3 of silicic magma that formed the present granite laccolith shortly after emplacement of the rim sill. The structural relief of the dome is 1.6 km, and the roof underwent 400 m of radial extension from the center. A crestal graben formed during doming, and the graben block collapsed less than 1 m.y. after formation of the dome, foundering and rotating down to the south after the roof was deeply eroded. The foundering of the crestal graben block was probably contemporaneous with the emplacement of a granite intrusion on the eastern side of the collapsed block and formation of a small caldera south of the crestal graben block. The series of intrusive and extrusive volcanic rocks found within the dome includes 14 mappable rock types, with a wide range of compositions. The Solitario igneous suite was emplaced over a total time span of 11 m.y.; silicic igneous activity was probably limited to the first 3 m.y. of this time. Younger, more mafic rocks have vents within the Solitario dome, and are thus included within the suite, but appear to be genetically and temporally related to the Bofecillos volcanic center, immediately west of the dome. The oldest units of the central basin-filling Needle Peak Tuff were deposited in late Eocene within 1 m.y. after the dome was formed. The roof of the dome was therefore eroded to virtually its present level by the end of the Eocene. The emplacement of the Needle Peak Tuff is associated, at least in part, with the collapse of a small caldera in the south part of the central basin. Volcaniclastic rocks accumulated in surrounding areas during the Oligocene and early Miocene, particularly those erupted from the Bofecillos volcanic center to the west. Early Oligocene Chisos Formation pinches out against the western flank of the dome. These volcanic units eventually lapped high onto the eroded rim of the dome, but did not spill over into the central basin. From early Miocene until the Quaternary, the area was an elevated plain, with the streams at or near their base level. There is no evidence in the map area for significant erosion or deposition from early Miocene until the Pleistocene, when the Rio Grande began actively downcutting its bed to the south. The base level of all local streams was lowered as a result. The map area is presently being rapidly eroded, and the late Eocene topography has been partially resurrected.
Igneous rocks of the Terlingua-Solitario region, Texas
Solitario uplift, Presidio-Brewster counties, Texas
The Circum-Laurentian Carbonate Bank, the Western Ouachita-Cuyania Basin, and the Prodigal Llanoria Landmass
Abstract Within the southern circum-Laurentian carbonate bank, a 1000-km-long × 550-km-wide (621 × 342 mi) basin, the Ouachita-Cuyania Basin, developed during the Cambrian-Middle Ordovi-cian. The western Ouachita-Cuyania Basin, including the Marathon-Solitario subbasin (west Texas), was flanked by fully correlative platform carbonate successions on the southern margin, as well as on the north. The southern carbonate complex, with its homologous sponge-algal reef organisms, is now preserved in the Cuyania terrane (greater Precordillera of Argentina). The Marathon-Solitario subbasin and Cuyania, with common fundaments of Laurentian Meso-proterozoic (Grenvillian) basement, evolved together, as evidenced by isotopic, lithostratigraph-ic, biostratigraphic, and chronostratigraphic data, as well as by new high-precision paleo-magnetic determinations. Ages, lead-isotopic data, and geochemical data for Cuyania and for west-central Texas crystalline basement rocks, particularly the Llano uplift and the Pecos mafic intrusive complex, are markedly similar. Mesoproterozoic through Eocambrian rocks of the central and western Ouachita embayment furnished detrital zircons to Cambrian siliciclastic deposits in the Precordillera. Faunas of the carbonate platform sequences that developed on both sides (e.g., El Paso and Chica de Zonda) of the basin were particularly well developed around the Laurentian Ouachita margin. The Marathon-Solitario subbasin received sediments from both north and south; much detritus came from the northern shelf, as well as from elevated blocks within the basin, and included decimeter-scale olistoliths bearing a shelf fauna. Ero-sional gaps on the platform correlate with intervals of coarse carbonate detritus in the basin. Cuyania constituted the vanished early Paleozoic landmass of Llanoria, the long-sought southern source for volcaniclastic, metaigneous, and metasedimentary detritus—most probably the Famatina eruptive complex and western Sierras Pampeanas—in siliciclastic deposits of the Marathon succession. Newly discovered pyroclastics and igneous rocks in the Marathon Formation suggest that coeval volcanic vents may also have developed on the western Ouachita margin during separation of Cuyania from Laurentia. Extensional block faulting, variable carbonate platform and outer-shelf and/or slope sedimentation, and explosive volcanism characterized the western Ouachita-Cuyania Basin from the Cambrian into the Middle Ordovician. Stratigraphy and structures of the basin are consonant with paleomagnetically derived plate reconstructions for that period, which place Cuyania and western Gondwana at low southern latitudes (∼26°S) and adjacent to southern Laurentia (omitting most of Mexico). The western Gondwanan margin trended west, that is, about 90° clockwise from its present orientation, and faced southern Laurentia. The Ouachita-Cuyania Basin was thus positioned to receive sediments from both Gondwana on the south and Laurentia on the north. The biostratigraphic data can readily be accommodated through faunal interchange by means of equator-parallel currents. During the Sandbian, Cuyania moved beyond range of faunal exchange with Laurentia, and tholeiitic basalts with enriched mid-ocean ridge basalt (E-MORB) characteristics were intruded into off-shelf turbidites down the length of the western Precordillera. The attenuated Laurentian slab broke apart with continued oblique dextral (transtensional) separation of Laurentia and Gondwana, and the early Paleozoic Llanoria landmass departed with the southern megacontinent. Geochronologic, paleomagnetic, and biostratigraphic data all attest to accretion of Cuyania to Gondwana well before the onset of Taconic orogenesis in eastern Laurentia.
STRATIGRAPHY AND PETROLOGY OF THE TASCOTAL MESA QUADRANGLE, TEXAS
▴ Geographic setting of the Solitario Canyon fault and the designated site ...
—Cerro Solitario seen from the south. Beds dip east (to right). Stratigraph...
Sensitivity Study of Physical Limits on Ground Motion at Yucca Mountain
Late Quaternary geomorphology and soils in Crater Flat, Yucca Mountain area, southern Nevada
Stratigraphy and sedimentary history of Pre-Permian Paleozoic rocks of the Marathon uplift
Abstract Paleozoic rocks that were deposited along the southeastern margin of North America during Paleozoic time and that make up the Ouachita orogen extend from Arkansas across Oklahoma and Texas and have been traced almost to Mexico. Rocks at the southwestern end of the Ouachita orogen are exposed only in the Marathon and Solitario uplifts in west Texas, but the western edge of the sequence in the subsurface of Texas is fairly well known from well and seismic data (e.g., Flawn and others, 1961; Nicholas and Rozendal, 1975). The Marathon uplift is a broad domal uplift of early Tertiary age and is more than 125 km in diameter (King, 1937). Erosion of Cretaceous and younger strata from the crest of the uplift produced the topographic Marathon Basin in which are exposed, in an area approximately 50 by 75 km, deformed Paleozoic rocks that have a composite stratigraphic thickness of 5000 m. Permian strata in the Glass Mountains unconformably overlie older rocks alongthe northwestern edge of the Marathon uplift (Fig. 1). The Solitario uplift, 65 km to the southwest, provides exposures of Paleozoic rock approximately 8 by 15 km at the crest of a buried intrusion.