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Analogue Model of Inversion Tectonics Explaining the Structural Diversity of Late Cretaceous Shortening in Southwestern Mexico

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Analogue Model of Inversion Tectonics Explaining the Structural Diversity of Late Cretaceous Shortening in Southwestern Mexico Analogue model of inversion tectonics explaining the structural diversity of Late Cretaceous shortening in southwestern Mexico Mariano Cerca1,*, Luca Ferrari1, Giacomo Corti2, Marco Bonini2, and Piero Manetti2 1CENTRO DE GEOCIENCIAS, UNIVERSIDAD NACIONAL AUTÓNOMA DE MÉXICO, CAMPUS JURIQUILLA, APARTADO POSTAL 1-742, QUERÉTARO 76230, MÉXICO 2CONSIGLIO NAZIONALE DELLE RICERCHE, ISTITUTO DI GEOSCIENZE E GEORISORSE, UNITÀ OPERATIVA DI FIRENZE, VIA G. LA PIRA, 4, 50121 FIRENZE, ITALY ABSTRACT The Laramide fold-and-thrust belt in southern Mexico is characterized by N-S–trending structures in its central and eastern part and by NW-SE–trending structures in its western part. Here, we investigate, experimentally, the possibility that the Laramide structures of southern Mexico may be the result of inversion of previously thinned lithosphere zones under oblique compression. A revision of the geology of this region shows that the presence of two extensional basins, representing relatively weak blocks within more rigid lithosphere, strongly controlled the subsequent deformation pattern. For modeling purposes, we divided the southern Mexico lithosphere into blocks with differ- ent strength profi les: (1) a stable craton; (2) a weak block composed of the Guerrero Morelos Platform; (3) a relatively strong block exposing the pre-Cretaceous Tejupilco schist and the Early Cretaceous Teloloapan volcanic arc (Tejupilco anticlinorium); and (4) a weak block repre- sented by the Arcelia–Palmar Chico basin. A series of physical experiments simulating the mechanical response of an analogue lithosphere composed of fi ve simplifi ed strength profi les was constructed. The model lithosphere was thinned orthogonally and shortened obliquely. Shortening was accommodated mainly by reactivation of preexisting extensional structures. The resulting orogenic deformation in the models is not entirely sequential and foreland-progressive. Inversion tectonics of extensional basins is thus proposed as an explanation for the structural diversity observed in Late Cretaceous shortening of southwestern Mexico. The predictions of our lithospheric model may be tested when more geophysical information about the structure of the southern Mexico lithosphere becomes available. LITHOSPHERE; v. 2; no. 3; p. 172–187. doi: 10.1130/L48.1 INTRODUCTION platform sequence during Albian–Turonian GEOLOGICAL EVOLUTION OF (Morelos Forma tion; Cerca et al., 2007); and SOUTHWESTERN MEXICO DURING THE Late Cretaceous Laramide shortening defor- (2) the Arcelia–Palmar Chico deep basin, which EARLY AND LATE CRETACEOUS mation in southern Mexico occurred primarily is characterized by a fl ysch-like sequence dur- through large-scale folds and thrusts involv- ing the Valanginian–Aptian and an alternating Recent work has provided a wealth of new ing Early Cretaceous and older rocks. These sequence of limestone and dominantly mid- information on the geology of southern Mexico structures strike N-S in an E-W section of more ocean-ridge basalt (MORB)–type volcanism (Cerca et al., 2007; Talavera-Mendoza et al., than 160 km between Ciudad Altamirano and during the Aptian–Coniacian (Arcelia–Palmar 2007; Solari et al., 2007; Centeno-García et Papalutla (Cerca et al., 2007; Martini et al., Chico Group; Martini et al., 2009). These al., 2008; Martini et al., 2009; Mortensen et al., 2009) and NW-SE farther to the west, NW of two basins are separated by a block expos- 2008). Southern Mexico geology is character- Zihuatanejo (Martini, 2008) (Fig. 1). The avail- ing the pre-Cretaceous metamorphic basement ized by a fi nite number of different terranes or able geological information from southern of the Tejupilco schist (Fig. 1) and the major subterranes that can be recognized by a detailed Mexico consistently suggests the occurrence Early Cretaceous Teloloapan volcanic arc. The analysis of the surface geology (Campa and of an episode of lithosphere thinning prior to scheme emerging from these fi rst-order observa- Coney, 1983; Sedlock et al., 1993; Tardy et al., Late Cretaceous shortening (e.g., Centeno- tions suggests that, as in many orogenic zones, 1994; Dickinson and Lawton, 2001; Keppie, García et al., 2008; Martini et al., 2009, and inversion of extensional basins is an important 2004). We focus our work on an ~220-km-long references therein). At a regional scale, at least mechanism in controlling the style and geome- and ~70-km-wide, E-W–trending zone, with two zones with geological evidence of Early try of Laramide shortening. Furthermore, it may complete exposures of Cretaceous lithology and Cretaceous extension can be identifi ed from explain the occurrence of N-S–trending struc- structures, located to the west of the Paleozoic east to west (Fig. 1): (1) the Guerrero Morelos tures in the central and eastern part of the south- Acatlan complex (Figs. 2 and 3). Platform, which has a sedimentary record of ern Mexico Laramide belt and coast-parallel, The aforementioned papers provide a continental margin conglomerates and minor NW-SE–trending structures in the western part detailed reconstruction of the geological evo- volcanism during Hauterivian–Aptian (Zicapa of the belt (Fig. 1C). In this work, we experi- lution of the region, which is characterized by Formation), followed by a thick carbonaceous mentally investigate the possibility that the an Early Cretaceous extensional phase in the N-S–trending contractile structures may have Arcelia–Palmar Chico Basin and in the Guer- *Corresponding author e-mail: mcerca@geociencias formed as a result of positive inversion tectonics rero Morelos Platform, predating the Laramide .unam.mx. during a phase of oblique compression. shortening. Based on these observations, we 172 For permission to copy, contact [email protected] | |Volume © 2010 2 Geological | Number Society3 | LITHOSPHERE of America Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/2/3/172/3044439/172.pdf by guest on 30 September 2021 Analogue model of inversion tectonics | RESEARCH A 100°W 90°W C TRANS-MEXICANVOLCANICBELT NORTH Toluca AMERICA Puebla PLATE Cuernavaca ? APC 20°N Fig. 1b ? Sierra Madre GMP del Sur Ciudad Altamirano 18°N TA Papalutlathrust Chortis stable plateau COCOS PLATE block or craton TMVB Chilpancingo B Zihuatanejo study area Acapulco Ma G 18°N Fig. 1c GMP Mi Zihuatanejo Anticline 16°N Acapulco J GOLFO PACIFIC X O Thrust DE OCEAN PACIFIC Normal fault OCEAN 16°N MÉXICO 150 Km 150 Km Puerto Angel Strike-slip fault 100°W 98°W 96°W 100°W 98°W Figure 1. (A) The study area is located in the area known as Sierra Madre del Sur in southwestern Mexico. (B) The lithosphere of southern Mexico has been classifi ed into tectonostratigraphic basement terranes (Campa and Coney, 1983; Sedlock et al., 1993): G—Guerrero; Mi—Mixteco; O—Oaxaca; Ma—Maya; X—Xolapa; J—Juarez; the Guerrero Morelos Platform (GMP) has been consid- ered either part of the Guerrero or the Mixteco terranes. TMVB—Trans-Mexican volcanic belt. (C) Regional structures and blocks defi ned in this work: a stable plateau or craton, exposing the Paleozoic Acatlán complex; weak block composed of the Guerrero Morelos Platform (GMP); a relatively strong block exposing the pre-Cretaceous Tejupilco schist and the Early Cretaceous Teloloa- pan volcanic arc (Tejupilco anticlinorium [TA]); and a weak block represented by the Arcelia–Palmar Chico and Huetamo basin (APC). Dashed lines represent the limits of the Xolapa and Guerrero terranes proposed by Campa and Coney (1983). Solid gray line is the limit between the Guerrero Morelos Platform and the Xolapa complex; thick solid lines represent the areas where the Xolapa complex is thrust over the Guerrero Morelos Platform. Strike slip along the thrust trace was proposed by Silva-Romo (2008). propose a model in which inversion tectonics review of the geology of southern Mexico. the region is underlain by a continental base- played an important role in controlling the dif- In the following section, we discuss only the ment below the Arcelia–Palmar Chico sequence ferences observed in the strain localization and relevant data for construction of the model. (Elías-Herrera et al., 2000; Talavera-Mendoza deformation style observed in the Mesozoic Schematic stratigraphic columns and the rela- et al., 2007; Martini et al., 2009). Moreover, lithostratigraphy of these terranes. Recent papers tion between blocks and tectonic events are two large-scale batholiths of continental affi nity support a model in which the Mesozoic volcano- presented in Figure 3. are found on both sides of the Arcelia–Palmar sedimentary successions of the Guerrero terrane Chico basin: the Placeres del Oro intrusive were deposited directly on the thinned continen- Arcelia–Palmar Chico–Huetamo Basin (ca. 119 Ma; Martini et al., 2009) and the Tin- tal margin of the North American plate (Cerca gambato batholith (ca. 130 Ma; Garza-González et al., 2007; Centeno-García et al., 2008; Mar- The Arcelia–Palmar Chico Cretaceous basin Vélez, 2007; Martini et al., 2009). tini et al., 2009), leaving no space for accretion was built on extended continental lithosphere The Cretaceous history of subsidence of the of allochthonous terranes as the cause for Late and consists of the western Huetamo and east- Arcelia–Palmar Chico basin starts in the Late Cretaceous shortening. Thus, analogue models ern Arcelia–Palmar Chico areas, the lateral con- Jurassic or Early Cretaceous with apron sedi- of lithospheric scale were constructed to explore tinuity of which has been recently confi rmed by mentary deposits and volcanic rocks (Guerrero- the infl uence of lateral mechanical variations Martini et al. (2009). Cretaceous sequences were Suástegui, 1997) of poorly constrained age during successive phases of extension and com- clearly deposited above metasedimentary rocks (Angao Formation). A period of continuous pression on the structural style that resulted in of Triassic age in the Huetamo area (Centeno- subsidence and marine transgression in the late the upper crust. The relative strengths of blocks García et al., 2003, 2008; Talavera-Mendoza et Valanginian to Aptian is recorded by the San used in the model were inferred from the basis of al., 2007; Martini et al., 2009).
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