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Gravity-Induced Folding Off a Gneiss Dome Complex, Rincon Mountains, Arizona

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Gravity-Induced Folding Off a Gneiss Dome Complex, Rincon Mountains, Arizona Gravity-Induced Folding off a Gneiss Dome Complex, Rincon Mountains, Arizona GEORGE H. DAVIS Department of Geosciences, University of Arizona, Tucson, Arizona 85721 ABSTRACT rocks crop out in isolated, shallow-dipping Most of them suggested a northerly sheets (1 to 25 km2 in extent) around the directed thrusting during early to middle Detached isoclinal folds, overturned base of the Rincon Mountains (Fig. 2). The Tertiary time. Drewes (1971, 1973) pro- asymmetric folds, and unbroken cascades sedimentary rocks (and their metasedimen- posed that the Paleozoic and Mesozoic of recumbent folds pervade sheets of tary equivalents) rest subconcordantly rocks were transported at least 16 to 32 km sedimentary and metasedimentary rocks of upon the gently to moderately steeply dip- northeastward by regional thrusting during Paleozoic and Mesozoic age that occur ping surface of the granitic gneiss (Fig. 3). the Laramide orogeny. McColly (1961) and around the base of the Rincon Mountains This surface, which conforms in attitude to Arnold (1971) suggested that the folds and near Tucson, Arizona. The sheets of folded the foliation in the gneiss, locally is marked faults that they mapped in sedimentary rocks rest subconcordantly on the gently by grooves and slickensides and was rocks on the west and south flanks of the dipping surface of the granitic gneiss that mapped by Pashley (1966) as the Catalina Rincon Mountains formed during gravity composes much of the range. This surface, fault. gliding of the rocks off the granitic gneiss known as the Catalina fault, parallels the Low-angle tectonic movement has oc- during Miocene time. attitude of the foliation in the gneiss and is curred within the sheets of Paleozoic and The focus of this study is a determination folded about two macroscopic upright an- Mesozoic sedimentary rocks. The dynamics of the tectonic transport direction(s) of the tiforms and an intervening synform. of the low-angle displacement have been in- sheets of sedimentary rocks based on slip- The low-angle tectonic displacement terpreted both by regional compressional line orientations calculated for folds in reflected in the folds was brought about by overthrusting and local gravitational tec- those sheets. The results are compared to local gravitational tectonics. The slip-line tonics. Darton (1925), Moore and others existing transport models to determine directions inferred from the geometry of the (1941), Brennan (1957), Layton (1957), whether the fold-forming event(s) resulted fold arrays define a radial pattern centered Acker (1958), Kerns (1958), Weidner from regional overthrusting, from gravity on the Rincon Mountains. The forms of the (1958), and Pashley (1966) attributed the tectonics related to emplacement of the folds are consistent with the characteristics folds and faults in the foothills of the Rin- granitic gneiss, or from a combination of of gravity-induced folds. con Mountains to regional overthrusting. the two processes. Most of the gravity-induced folding is in- terpreted to have accompanied the 28- to 24-m.y. uplift that ended the Tertiary metamorphism of gneiss in the Rincon Mountain complex. The Catalina fault is interpreted to be a décollement, above which the sedimentary and metasedimen- tary rocks folded independently of their substratum. Key words: structural geology, gravity tectonics, folds, gneiss dome, struc- tural analysis. INTRODUCTION The Rincon Mountains near Tucson, Arizona (Fig. 1), which herein include the Tanque Verde Mountains, are composed predominantly of gneissic granitic rocks that have been folded into two large, open antiforms and an intervening synform. The limbs of these N. 60° E.—trending upright symmetrical folds dip on the average 15° to 20° (Fig. 2; Pashley, 1966). A north-striking high-angle normal fault of Miocene(?) to Pleistocene age (Drewes, 1971) truncates the folds to the east and defines the pre- cipitous eastern boundary of the Rincon Mountains (Fig. 2). Paleozoic and Mesozoic sedimentary Figure 1. Location map. Geological Society of America Bulletin, v. 86, p. 979-990, 11 figs., July 1975, Doc. no. 50715. 979 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/86/7/979/3433802/i0016-7606-86-7-979.pdf by guest on 30 September 2021 980 G. H. DAVIS MAJOR ROCK UNITS Rincon Valley Granite ronment in which the folds formed and thus be useful in distinguishing among the fold- Catalina Gneiss The Rincon Valley Granite was described forming tectonic processes mentioned by Moore and others (1941) as a medium- above. The term "Catalina Gneiss" was intro- to coarse-grained, greenish granitic rock The properties of folds in sedimentary duced by DuBois (1959) to refer to the composed of sericitized potassium feldspar, and metasedimentary rocks of Paleozoic gneissic granitic rocks that make up the oligoclase, and interstitial quartz with and Mesozoic age at five locations around core of the Rincon Mountains and the chloritized biotite. It is distinctive in the the Rincon Mountains were examined in Santa Catalina Mountains (Fig. 1). DuBois field because of its light greenish-brown/ this investigation. The areas range in areal (1959) divided the Catalina Gneiss into gray color on weathered surfaces and its extent from 1 to 25 km2 and include banded augen gneiss, augen gneiss, and highly shattered condition. The rock has Saguaro National Monument (Paleozoic granitic gneiss/gneissic granite. Mayo the composition of granodiorite and locally rocks), Loma Alta (Mesozoic rocks), Col- (1964) studied the cataclastic foliation that grades into quartz monzonite (Acker, ossal Cave (Paleozoic rocks), Martinez characterizes the banded gneiss in the 1958; Arnold, 1971). K-Ar age deter- Ranch (Paleozoic rocks), and Bear Creek forerange of the Catalina Mountains; he minations of 1,540 ± 60 m.y. obtained (Paleozoic and Mesozoic rocks) (Fig. 2). described it as consisting of aligned mica by Marvin and others (1973) indicate that Each represents a separate structural do- books and quartz and feldspar augen, ac- the Rincon Valley Granite is Precambrian. main characterized by essentially uniform centuated by layers and lenses of pegmatite, Drewes has mapped the "Rincon Valley bedding strike. Specific methods employed quartz lenses and sheets, dark coarse- Granodiorite" and considers it to represent in this study are described in Appendix 1. grained mica schist, and bands of porphy- an allochthonous plate, the middle of three riticorporphyroblastic rock. Drewes (1973, regional thrust plates (Drewes, 1971). Geometric Analysis personal commun.) has disclosed that the core rocks in the Rincon Mountains are Phanerozoic Sedimentary Rocks Saguaro National Monument. Sedi- petrologically more complex than previ- mentary rocks on the west side of the ously recognized. Among the mappable The Paleozoic sedimentary rocks in the Rincon Mountains within Saguaro Na- units that Drewes (1972) has distinguished foothills of the Rincon Mountains consist tional Monument (Fig. 2) consist of lime- are gneissic biotite-muscovite quartz mon- chiefly of limestone interbedded with lesser stone, dolomite, shale, and limestone con- zonite, porphyritic biotite-rich meta- amounts of siltstone and shale. An account glomerate of Permian(?) age (McColly, granodiorite, schist, and metadiorite or of the Paleozoic formations cited in this 1961), as well as remnants of Pennsylva- metadiabase. "Catalina Gneiss" is used paper is provided by Bryant (1968). nian, Cretaceous, and possibly Mississip- herein merely as a general term for the crys- Mesozoic rocks are sparse in the Rincon pian formations (Drewes, 1974, personal talline, granitic-gneissic rocks in the Rincon Mountain area (Fig. 2). They belong to the commun.). The rocks strike northeast, dip and Santa Catalina Mountains. Bisbee Group of Early Cretaceous age and northwest, and are essentially parallel to The age(s) of the rocks from which the have been mapped by Arnold (1971) in the upper surface of the underlying Cata- Catalina Gneiss was derived, the age(s) of Rincon Valley and by Drewes (1972) in lina Gneiss, which lies in the northwest metamorphism, and the age of macroscopic Happy Valley and in Saguaro National limb of the Tanque Verde antiform. Lime- folding in the Catalina Gneiss are uncer- Monument (Drewes, 1974, personal com- stone units are locally metamorphosed tain. Damon and others (1963) have con- mun.). along the sedimentary rock-gneiss contact. cluded, on the basis of (1) the spatial rela- Sedimentary rocks of the Tertiary Pan- Much of the field work centered on tion of the Catalina Gneiss to its mantle of tano Formation are exposed along much of analyzing folds in limestone and shale ex- younger Precambrian Apache Group rocks the margin of the Rincon Mountains, where posed on a steep south-facing hillside in the in the Catalina Mountains (Waag, 1968) they are characteristically moderately central part of the domain. McColly (1961) and (2) the 1,660-m.y. age derived from the steeply dipping and broken by abundant interpreted the structure there as a single lead isotopic content of zircon in the gneiss, normal faults (Brennan, 1957; Arnold, large recumbent fold. However, the rocks that most of the Catalina Gneiss was de- 1971). Dating demonstrates that the Pan- are replete with unbroken cascades of re- rived from older Precambrian rocks. The tano Formation includes rocks that are cumbent and overturned folds (Fig. 4). In- characteristic K-Ar ages of approximately pre—lower Oligocene and post—lower terbedded shale units are pervaded by a 27 m.y., obtained from mica in the gneiss, Miocene in age (Metz, 1963; Damon and bedding-plane cleavage and contain root- further suggested to Damon and others Bikerman, 1964; Damon and others, 1965, less isoclinal folds and S-shaped minor folds (1963) that the core rocks of the Santa 1966; Finnell, 1970). that are asymmetric basinward. Catalina—Rincon complex had been sub- Visual harmonic analysis of 23 individual jected to a Cretaceous-Tertiary metamor- FOLDS surfaces of folds revealed the relatively phic event that ended by late Oligocene broad shape-to-amplitude distribution to early Miocene time. Mayo attributed the The basis for the fold analysis used in this shown in Figure 5 (see Appendix 1).
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