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Strain and Magnetic Fabric in Santa Catalina and Pinaleno Mountains Metamorphic- Core- Complexes Mylonite Zones, Arizona Amy S

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Strain and Magnetic Fabric in Santa Catalina and Pinaleno Mountains Metamorphic- Core- Complexes Mylonite Zones, Arizona Amy S University of Portland Pilot Scholars Environmental Studies Faculty Publications and Environmental Studies Presentations 4-1988 Strain and Magnetic Fabric in Santa Catalina and Pinaleno Mountains Metamorphic- Core- Complexes Mylonite Zones, Arizona Amy S. Ruf Stephen J. Naruk Robert F. Butler University of Portland, [email protected] Gary J. Calderone Follow this and additional works at: http://pilotscholars.up.edu/env_facpubs Part of the Environmental Sciences Commons, and the Geophysics and Seismology Commons Citation: Pilot Scholars Version (Modified MLA Style) Ruf, Amy S.; Naruk, Stephen J.; Butler, Robert F.; and Calderone, Gary J., "Strain and Magnetic Fabric in Santa Catalina and Pinaleno Mountains Metamorphic- Core-Complexes Mylonite Zones, Arizona" (1988). Environmental Studies Faculty Publications and Presentations. 19. http://pilotscholars.up.edu/env_facpubs/19 This Journal Article is brought to you for free and open access by the Environmental Studies at Pilot Scholars. It has been accepted for inclusion in Environmental Studies Faculty Publications and Presentations by an authorized administrator of Pilot Scholars. For more information, please contact [email protected]. TECTONICS, VOL. 7, NO. 2, PAGES 235-248, APRIL 1988 STRAIN AND MAGNETIC FABRIC IN THE SANTA CATALINA AND PINA LENO MOUNTAINS METAM ORPHIC CORE COMPLEX MYLONITE ZONES, ARIZONA Amy S. Ruf, Stephen J. Naruk, 1 Robert F. Butler, and Gary J. Calderone2 Department of Geosciences, University of Arizona, Tucson Abstract. Anisotropy of magnetic susceptibility subsequent deformation. the long axes are rotated (AMS) is capable of recording finite strain in into the maximum extension direction. In the weakly magnetized rocks. AMS was measured for Pinaleno mylonites, both equant and elongate 228 samples from 20 sites in two mylonite zones magnetite grains are present. With deformation, with the same deformational history. AMS the elongate magnetite grains are rotated into the measurements were compared with finite strains maximum flattening plane but show no preferred determined from dike rotations and from foliation orientation within this plane. AMS in the two orientations. In one zone (the Santa Catalina mylonite zones appears to be predominantly Mountains) the orientations of susceptibility and controlled by the orientation of elongate magnetite finite strain ellipsoids are in excellent agreement, grains with respect to the megascopic fabric. The and there is a logarithmic relationship between fina1 orientation of the elongate grains is a susceptibility difference (.6.Ki .a {K1-K]/K) and function of their initial orientation as well as the finite strain magnitude. In the second zone (the finite strain. Therefore, despite similar Pinaleno Mountains) minimum susceptibility is deformational histories, the two zones display perpendicular to the finite flattening plane. but the different AMS patterns due to the differences in maximum susceptibility does not parallel the occurrence, initial orientation, and shape of maximum extension direction, and there is no ferromagnetic grains. systematic relationship between susceptibility magnitude and strain magnitude. Oriented polished INTRODUCTION thin sections indicate that magnetite in the protolith of the Santa Catalina mylonite occurs as randomly oriented, elongate grains. With Both anisotropy of magnetic susceptibility (AMS) and strain are second order tensors geometrically represented by ellipsoids. Many recent investigations of AMS and strain have estabHshed a general coincidence of the principal axes of the 1Now at Shell Western E & P Inc., Houston, magnetic fabric and petrofabric ellipsoids, with the Texas. maximum susceptibHity axis oriented para1lel to 2Also at U.S. Geological Survey, Flagstaff, petrographic lineation and the minimum Arizona. susceptibility axis oriented perpendicular to foHation [Goldstein and Brown, I 986; Rathore, 1985; Copyright 1988 Kligfield et al., 1983; Rathore et al., 1983] (and by the American Geophysical U nioo review by Hrouda [1982]). Such studies have been carried out in sedimentary rocks {e.g., Graham, Paper number 7T084I. 1966; Kligfield et al., 1977, 1982], igneous rocks 0278-7407 /88/007T-0841$10.00 [e.g., Rathore, 1980, 1985], and metamorphic rocks 236 Ruf et al.: Strain and Magnetic Fabric in Mylonites 10 KM Holt et. at, 1986 ~ penetratively mylonitized rocks of lower plate upper-plate rocks . Tertiary plutonic and sedimentary rocks, Paleozoic, • . Cretaceous and late Precambrian sediments Precambrian Oracle quartz monzonite ~ intruded by Tw - fault ...u.--r.i... detachment fault .t-J- normal fault Fig. la. Geologic map of the Santa Catalina-Rincon Mountains metamorphic core complex, showing AMS site locations (triangles). Tw, Wilderness granite. (Modified from Holt et al. [J 986]). [e.g., Goldstein, 1980; Goldstein and Brown, 1986). and Brown, 1986; Rathore et al., 1983; Goldstein, This report discusses the applicability of AMS as a 1980]. However. in none of these studies has strain indicator in ductilely deformed granitic detailed strain control such as that included in the rocks in the mylonite zones of the Santa Catalina present study been available. Thls research was and Pinaleno Mountains metamorphic core initiated with two particular goals in mind: ( J) to complexes (Figure 1). two mylonite zones for which characterize strain in the mylonite zones in terms the deformational histories and finite strain values of AMS data and (2) to examine the development are known [Naruk, 1986a, b, l987a, b]. of magnetic anisotropy in the mylonite zones with Previous AMS studies have suggested that it is increasing strain. possible to obtain complete strain ellipsoid data The Santa Catalina and Pinaleno Mountains are from the magnetic susceptibility ellipsoid, which two of approximately 25 North American mountain can be measured rapidly and accurately [Goldstein ranges identified as Cordilleran metamorphic core Ruf et al.: Strain and Magnetic Fabric in Mylonites 237 1 1 KM, penetratively mylonitized ~ rocks of lower plate D alluvium quartzofeldspathic gneiss ~....... 1-,,,,!~;:(~ granite g biotite schist 12].> granodiorite .,,,.- 111:.,.....,~, / shear zone boundary ,, •• t. porphyritic gneiss Fig. lb. Geologic map of the Pinaleno Mountains mylonite zone, showing AMS site locations (PNJ-PN6). complexes [Davis and Coney, 1979; Crittenden et The Santa Catalina zone cuts across and al., 1980]. The mylonite zones of both the Santa displaces a suite of petrologically distinct dikes. Catalina and Pinaleno Mountains are low-dipping, These dikes have a uniform orientation in the normal displacement zones of pervasively foliated undeformed state, as well as uniform, but different, and lineated s-c (foliated with shear bands) orientations in the deformed state. The shear mylonites. The lower boundaries of both zones are strain (1) within the Santa Catalina zone fa related gradational contacts between the mylonites and to the orientation of these dikes by the following their undeformed granitic equivalents. These equation [Ramsay, 1967] (see Figure 3): transitions between undeformed rocks and mylonites provide a significant strain gradient '1 = cot a' - cot a: (l) within which to examine the development of magnetic anisotropy (Figure 2). Furthermore, the where finite strains and deformational histories of these '1 = tan t/J zones are already known in significant detail [Naruk, I 986a, b, 1987a, b ], thus providing the and basis for a controlled comparison of AMS and t/J = angular shear strain data. n' = the angle, measured in the XZ plane, between the deformed dike and the shear zone boundary, STRAIN DETERMINATIONS and a = the angle, also measured in the XZ plane, between the undeformed dike and the shear zone Both the Santa Catalina and Pinaleno mylonite boundary. zones are zones of simple shear deformation, and In simple shear, the XY plane of the finite both have well-defined planar lower boundaries. In strain ellipsoid rotates as a function of shear both zones the mylonitic foliation surfaces are strain magnitude. Specifically, the angle (O') discordant to the zone boundary and parallel to between the XY plane and the shear zone boundary the XY surface of the finite strain ellipsoid (axes is an inverse function of the shear strain [Ramsay X~.Y~Z) (Naruk, 1986a, b, 1987a, b]. and Graham, I 970]: 238 Ruf et al.: Strain and Magnetic Fabric in Mylonites angles between the foliation and the shear zone boundary for 6' (see Table 1). FIELD AND LABORATORY METHODS FOR AMS MEASUREMENT In both areas, samples for AMS measurement were collected from undeformed granite and from deformed granite, with each of the deformed sites representing a different degree of strain. In the Santa Catalina zone in particular, samples were collected from one site in undeformed granite r--- a) b) I-~ I I I l Fig. 2. Schematic diagram of a metamorphic core complex. (a) nonmylonitic core, (b) mylonite zone, (c) altered breccias. (d) detachment fault. (e) brittlely extended upper plate. The transition from A A' Figure 2a to 2b represents a significant strain Windy Point (CM) gradient from essentially undeformed rocks to their c) \ mylonitic equivalents. This gradient provides the basis for a controlled comparison of AMS and strain data. 1 mile Fig. 3. Schematic block diagrams of simple shear "I = 2 cot (20') (2) strain equations. No strain occurs perpendicular to = the p1ane of the figure (e7 0). (a) Undeformed Thus, where the orientation of the XY surface is state. The strain ellipse is represented by the known, 1 can be
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