Magnetic Polarity Stratigraphy of the Early Tertiary Black Peaks Formation, Big Bend National Park, Texas

Rapp, Stephen D.; MacFadden, Bruce J.; Schiebout, Judith A.

doi:10.1086/628804

Cited by 59 publications

(20 citation statements)

References 16 publications

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“…The consistent discrepancy of temporal correlations between the San Juan Basin sequence and those in other areas, at both the top (Butler et al 1981b;Rapp et al 1983; see above) and bottom (Lerbekmo et al 1979 a andAlvarez & Vann 1979;Fassett 1979;Lucas & Rigby 1979;Orth et al 1981 a and b;Lucas & Schoch 1982; see above) of the section, have forced us to re-evaluate the San Juan Basin magnetostratigraphic correlations. Faunal and magnetostratigraphic correlations to the time-scale in both the upper and lower parts of the San Juan Basin sequence are younger than those from other areas.…”

Section: I55mentioning

confidence: 95%

Jurassic to Paleogene: Part 2 Paleogene geochronology and chronostratigraphy

Berggren

Kent²,

Flynn

1985

Memoirs

313

592

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S U M M A R Y :We present a revised Paleogene geochronology based upon a best fit to selected high temperature radiometric dates on a number of identified magnetic polarity chrons (within the late Cretaceous, Paleogene and Neogene) which minimizes apparent accelerations in sea-floor spreading. An assessment of first order correlations of calcareous plankton biostratigraphic datum events to magnetic polarity stratigraphy yields the following estimated magnetobiochronology of major chronostratigraphic boundaries: Cretaceous-Tertiary boundary (Chron C29R), 66.4 Ma; Paleocene-Eocene (Chron C24R), 57.8 Ma; Eocene-Oligocene (Chron C13R), 36.6 Ma; Oligocene-Miocene (Chron C6CN), 23.7 Ma.The Eocene is seen to have expanded chronologically (-21 m.y.) at the expense of the Paleocene (-9 m.y.) and is indeed the longest of the Cenozoic epochs. In addition, magnetobiostratigraphic correlations require adjustments in apparent correlations with standard marine stage boundaries in some cases (particularly in the Oligocene). Finally, we present a correlation between standard Paleogene marine and terrestrial stratigraphies.It is nearly 20 years since Brian Funnell prepared the first relatively precise Cenozoic time-scale based on an assessment of palaeontologically controlled radiometric data in connection with the symposium on the Phanerozoic timescale sponsored by the London Geological Society, and 10 years since one of us (WAB) presented the first in a series of attempts to further refine Cenozoic geochronology. During the past decade several revisions to the Cenozoic time-scale have appeared and here, at this, the second symposium on the Phanerozoic time-scale sponsored by the Geological Society of London, it is appropriate to present an updated and, hopefully, improved version of the Cenozoic time-scale.It is opportune that over the past decade direct correlation has been achieved between plankton biostratigraphy in some of the standard European continental marine sections and North American terrestrial vertebrate biochronology and magnetic polarity stratigraphy over much of the Cenozoic Era. The recent improvement in deep sea coring techniques has further extended these correlations on a global scale. It is now possible to make age estimates of epoch boundaries and the extent of time-stratigraphic (standard ages) units in terms of plankton biostratigraphy and magnetic polarity chrons and/or anomalies.Finally a critical evaluation must be made within a geohistorical context of biostratigraphically controlled radiometric dates and radiometrically dated polarity stratigraphy in order to provide constraints on an internally consistent geologic time-scale.The revised Cenozoic geochronology has been prepared in two parts: (a) Paleogene; (b) Neogene. In this paper dealing with the Paleogene we first discuss the development of geomagnetic polarity history of the late Cretaceous and Cenozoic. A revised geochronology is then presented which is based upon a best fit to selected high temperature radiometric dates on a number of identifi...

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Section: I55mentioning

confidence: 95%

Jurassic to Paleogene: Part 2 Paleogene geochronology and chronostratigraphy

Berggren

Kent²,

Flynn

1985

Memoirs

313

592

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“…4) were taken. age control of any K-T exposures in the Tornillo Basin, having been dated by previous vertebrate biostratigraphic and magnetostratigraphic studies (Wilson 1970;Schiebout 1974;Rapp et al 1983;Lehman 1985a;Standhardt 1986;and Runkel 1988as cited in Lehman 1989, 1990, and 1991. The Aguja and Javelina formations occur within the Upper Cretaceous Judithian, Edmontonian, and Lancian North American Land-Mammal Ages, whereas the Black Peaks Formation is of Paleocene Puercan age (Fig.…”

Section: Stratigraphic Overview and Paleogeographymentioning

confidence: 99%

Eustatic Control on Alluvial Sequence Stratigraphy: A Possible Example from the Cretaceous-Tertiary Transition of the Tornillo Basin, Big Bend National Park, West Texas, U.S.A.

Atchley¹,

Nordt²,

Dworkin³

2004

Journal of Sedimentary Research

104

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Paleosol-bearing alluvial strata of latest Cretaceous and earliest Tertiary age are continuously exposed along Dawson Creek, in Big Bend National Park, west Texas, U.S.A., and exhibit a three-tier hierarchy of depositional cyclicity. Meter-scale, fluvial aggradational cycles (FACs) occur as fining-upward successions that are gradationally overlain by paleosols or are sharply overlain by the coarsergrained base of the succeeding FAC without an intervening paleosol. FACs stack into decameter-scale, fluvial aggradational cycle sets (FAC sets) that also fine upward, and from base to top contain either a gradual upsection increase in soil maturity and soil drainage or a somewhat symmetrical pattern of increasing and decreasing paleosol maturity. Longer-period trends of FAC thickness, lithologic proportions, paleosol maturity, and paleosol drainage indicate that two complete, and two partial, hectometer-scale fluvial sequences occur within the study interval. From base to top, each sequence is characterized by an asymmetric increase and decrease in FAC thickness, a decrease in the proportion of sand-prone fluvial facies, an increase in paleosol maturity, and better paleosol drainage. Whereas FACs and FAC sets are interpreted to record cyclic episodes of channel avulsion and stability, and longer-term avulsive channel drift within the alluvial valley, respectively, fluvial sequences may coincide with third-order sea-level changes within the North American Western Interior Seaway. As such, the Cretaceous-Tertiary (K-T)transition within the Tornillo Basin may provide an example of megascale stratigraphic cyclicity that is controlled by eustatic sea level within a fully fluvial succession. Thickening and thinning successions of FACs record a third-order period of accelerating (transgressiveequivalent) and decelerating (highstand-equivalent) base-level rise, and subsequent base-level fall (falling stage-to lowstand-equivalent). Sequence boundaries are placed at the sharp inflection between thinning and thickening FACs. Sand-prone facies and immature, more poorlydrained paleosols are associated with the transgressive-equivalent portion of each sequence, and mudrock-dominated overbank facies and their associated mature, well-drained paleosols are associated with the highstand-and falling stage-equivalent.

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“…This magnetic record, located along the basalt-capped escarpment ~20 km west of Long Point, closely matches the pole position of Chron 24 (ca. 56-53 Ma), as measured in the Black Peaks Formation of Texas (Rapp et al, 1983;Elston et al, 1989). Chron 24 is known to include 5 or more normal and reversed intervals, with lengths as short as 40-70 k.y.…”

Section: Summary Of Evidence For Stratigraphic Range Of the Music Moumentioning

confidence: 99%

Paleogene rim gravel of Arizona: Age and significance of the Music Mountain Formation

Young

Hartman

2014

Geosphere

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The early Tertiary exotic rim gravel scattered across the Colorado Plateau in Arizona (USA) provides the only widespread evidence concerning the nature of the regional Paleogene drainage system that preceded the emergence of the modern Colorado River. The term "rim gravel" includes a wide range of Laramide (herein ca. 85-40 Ma) and younger reworked quartzite-dominated, arkosic sediments with diverse origins and ages that have been clarifi ed only recently. The parent arkoses, with subordinate gravel lenses, contain volcanic clasts with ages ranging from Late Jurassic to early Eocene. The Laramide-age arkoses were shed off uplifted Precambrian terranes to the south and west; they are separated from their reworked derivatives and younger sediments by a disconformity that is best preserved in the structurally isolated paleocanyons of the Hualapai Plateau. Younger generations of reworked gravels continued to evolve during and following the widespread eruption of basalts of late Oligocene to Pleistocene age. Basaltic clasts in the reworked gravels attest to their much younger ages. Combined paleontologic, stratigraphic, paleomagnetic, K-Ar, U-Th/He, and zircon studies of the parent arkoses indicate that the tectonic framework corresponds to the Laramide orogeny, the concurrent regional erosion of the Colorado Plateau margin, and ensuing widespread deposition. The overall time frame coincides with the similar tectonic history recorded in the early Tertiary strata of southern Utah. Comparable but unrelated quartzite-dominated gravels, reworked southward from the Utah source rocks, are widespread on strath terraces north of the Colorado River.

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Magnetic Polarity Stratigraphy of the Early Tertiary Black Peaks Formation, Big Bend National Park, Texas

Cited by 59 publications

References 16 publications

Jurassic to Paleogene: Part 2 Paleogene geochronology and chronostratigraphy

Jurassic to Paleogene: Part 2 Paleogene geochronology and chronostratigraphy

Eustatic Control on Alluvial Sequence Stratigraphy: A Possible Example from the Cretaceous-Tertiary Transition of the Tornillo Basin, Big Bend National Park, West Texas, U.S.A.

Paleogene rim gravel of Arizona: Age and significance of the Music Mountain Formation

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