Miocene extension and fault-related folding in the Highland Range, southern Nevada: a three-dimensional perspective

Faulds, James E.; Olson, Eric L; Harlan, Stephen S.; McIntosh, William C.

doi:10.1016/s0191-8141(01)00116-x

Cited by 38 publications

(55 citation statements)

References 61 publications

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“…It is suggested that such stress field is generally characteristic for the late-stage evolution of the Sirt Basin (Morley et al, 1990;Marović , 2007). The structural geometry is controlled by normal faults and extensional fault-related folds, similar to the geometry of numerous rift zones (Morley et al, 1990;Koledoye et al, 2000;Faulds et al, 2002). Degree of deformation implies that the intensity of extensional deformations gradually decreased from the Eocene to Lower Miocene.…”

Section: Pre-volcanic Basement and Regional Stress Fieldmentioning

confidence: 98%

Petrogenesis of the eastern part of the Al Haruj basalts (Libya)

Cvetković

Toljić

Ammar

et al. 2010

Journal of African Earth Sciences

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Section: Pre-volcanic Basement and Regional Stress Fieldmentioning

confidence: 98%

Petrogenesis of the eastern part of the Al Haruj basalts (Libya)

Cvetković

Toljić

Ammar

et al. 2010

Journal of African Earth Sciences

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“…7B). Younger clusters of high-K index volcanics in the CREC, erupted between 18 and 12 Ma, coincide with extensional faulting that Faulds et al (2002) ascribed to a period of major extension between 16.5 and 11 Ma (between 35 and 36°N).…”

Section: Volcanism As Controlled By Crustal Extensionmentioning

confidence: 96%

“…Our qualitative cross section (Fig. 9A) is based on geophysical results (Goes and van der Lee, 2002) (Fridrich et al, 1998) Acceleration of MCC exhumation (Anderson et al, 1988) Detachment Faults (Beratan & Nielsen, 1996) Extensional faulting (Faulds et al, 2002) Extension in southeast CA (Jacobsen et al, 2002) W (Duebendorfer & Simpson, 1994) Post-8.5 Ma extension? (Duebendorfer & Simpson, 1994) on April 3, 2013 geosphere.gsapubs.org Downloaded from thickens from west to east.…”

Section: Active or Passive Mantle Upwelling?mentioning

confidence: 99%

Basin and Range volcanism as a passive response to extensional tectonics

Putirka

Platt

2012

Geosphere

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A long-standing issue in Cordilleran geology involves the nature of Basin and Range (western USA) volcanism, and whether such magmatism provides a trigger for extensional deformation, or if volcanic activity is a passive response to extension. We use space-timecomposition patterns across the central and southern Basin and Range, and where appropriate, reconstructed latitudes and longitudes of volcanic rocks, to show that volcanism is fundamentally a passive process. Our analysis suggests that Basin and Range volcanism is initiated by the transition from a subduction to a transform boundary (now manifest as the San Andreas fault), which causes a slab window to open, as the subducting Farallon plate falls away. Accordingly, volcanic activity follows the northward-migrating Mendocino Triple Junction (MTJ). In the wake of the MTJ, continental mantle lithosphere is heated over a time scale of 10-12 Ma; it then rapidly degrades (or is removed) 17-20 Ma after MTJ arrival at any given latitude, and is replaced by asthenosphere. In the central Basin and Range, MTJ migration triggers the well-documented structural migration of the Sierra Nevada away from the Colorado Plateau. Not only is volcanism triggered by the tectonic transition, but in the central Basin and Range volcanism also migrates west, following the initiation of upper crustal extensional faulting; the lag between the onset of extension and initiation of volcanism is a remarkably consistent 2 Ma. Within this framework, the initial stage of eastward-concentrated volcanism is dominated by felsic magmatism, which then gradually degrades to a more mafi c composition. This pattern, and temporal relations indicate that once lithospheric extension begins, between 2 and 5 Ma are needed to develop conduits through which nonviscous magmas can transit the crust, and that especially high amounts of extensional strain favor the eruption of K 2 Orich, low-degree partial melts. Our observations indicate that it is unlikely that mantle plume processes initiated Basin and Range volcanism within the study area, and that decreases in SiO 2 and increases in incompatible element abundances to the east within the Cordillera are best explained by continental mantle lithosphere that thickens to the east, which reduces average melt fractions.

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“…There are thick volcanic sequences of appropriate age that have erupted from the Aztec Wash chamber in nearby areas of southern Nevada and north-western Arizona (Gans et al 1989(Gans et al , 1992Faulds et al 2001Faulds et al , 2002Metcalf 2004). What are the processes that trigger eruptions and how are they manifested in the plutonic record?…”

Section: Plutons and The Subsurface Record Of Eruption And Magma Filtmentioning

confidence: 99%

Granites, dynamic magma chamber processes and pluton construction: the Aztec Wash pluton, Eldorado Mountains, Nevada, USA

Harper

Miller

Koteas

et al. 2004

Earth and Environmental Science Transactions of the Royal Socie

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The mid-Miocene Aztec Wash pluton is divisible into a relatively homogeneous portion entirely comprising granites (the G zone, or GZ), and an extremely heterogeneous zone (HZ) that includes the products of the mingling, mixing and fractional crystallisation of mafic and felsic magmas. Though far less variable than the HZ, the GZ nonetheless records a dynamic history characterised by cyclic deposition of the solidifying products of the felsic portion of a recharging, open-system magma chamber. Tilting has exposed a 5-km section through the GZ and adjacent portions of the HZ. A porphyry is interpreted as a remnant of a chilled roof zone that marks the first stage of felsic GZ intrusion. Subsequent recharging by felsic and mafic magma, reflected by repeated cycles of crystal accumulation and melt segregation in the GZ and emplacement of mafic flows in the HZ, rejuvenated and maintained the chamber. Kilometre-scale lobes of mafic HZ material were deposited as prograding tongues into the GZ during periods of increased mafic input. Thus, they are lateral equivalents of the cumulate GZ granites with which they interfinger. Conglomerate-like units comprising rounded, matrix-supported intermediate clasts in cumulate granite are located immediately above the lobes. These 'conglomerates' appear to represent debris flows shed from sloping upper surfaces of the lobes. Thus, the GZ can be viewed as comprising distal facies, remote from the site of mafic recharging in the HZ, and the HZ as comprising proximal facies.Elemental chemistry suggests that the GZ cumulate granites represent a second-stage accumulation from an already evolved melt, and that coarse, more mafic, feldspar+biotite+accessory mineral hornblende rocks trapped between mafic sheets in the HZ are the initial cumulates. Fractionated melt accumulated roofward and laterally, and was the direct parent of the 'evolved' GZ cumulates. The most highly fractionated, fluid-rich melts accumulated at the roof.

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Miocene extension and fault-related folding in the Highland Range, southern Nevada: a three-dimensional perspective

Cited by 38 publications

References 61 publications

Petrogenesis of the eastern part of the Al Haruj basalts (Libya)

Petrogenesis of the eastern part of the Al Haruj basalts (Libya)

Basin and Range volcanism as a passive response to extensional tectonics

Granites, dynamic magma chamber processes and pluton construction: the Aztec Wash pluton, Eldorado Mountains, Nevada, USA

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