The Guerrero Composite Terrane of western Mexico

Transcription

The Geological Society of America
Special Paper 436
2008
The Guerrero Composite Terrane of western Mexico: Collision and
subsequent rifting in a supra-subduction zone
E. Centeno-García*
Instituto de Geología, Universidad Nacional Autónoma de México, Ciudad Universitaria, México D.F. 04510, México
M. Guerrero-Suastegui
O. Talavera-Mendoza
Unidad Académica de Ciencias de la Tierra, Universidad Autónoma de Guerrero, AP 197, Taxco el Viejo, Guerrero, México
ABSTRACT
The Guerrero Composite Terrane of western Mexico is the second largest terrane in North America. Mostly characterized by submarine volcanism and formed
by five terranes, the Guerrero records vast and complex subduction-related processes
influenced by major translation and rifting. It is composed of the Teloloapan, Guanajuato, Arcelia, Tahue, and Zihuatanejo Terranes. The Teloloapan Terrane is made
up of Lower Cretaceous island-arc (IA) andesitic to basaltic submarine lava flows,
interbedded with limestone and shallow-marine volcaniclastic rocks. The Guanajuato
and Arcelia Terranes are characterized by Lower Cretaceous supra-subduction
ophiolite successions formed by deep-marine volcanic and sedimentary rocks with
mid-oceanic-ridge basalt (MORB), oceanic-island basalt (OIB), and island-arc basalt
(IAB) signatures. These two terranes are placed between the continent and the more
evolved arc assemblages of the Zihuatanejo Terrane. The Tahue Terrane is composed
of Paleozoic accreted arc and eugeoclinal sedimentary rocks, Triassic rift-related
metaigneous rocks, and overlain unconformably by pillow basalts, limestone, and
volcaniclastic rocks. The Zihuatanejo Terrane was formed by Triassic ocean-flank to
ocean-floor assemblages accreted in Early Jurassic time (subduction complexes). The
subduction complexes are overlain by Middle Jurassic–evolved volcanic arc rocks,
which are in turn unconformably overlain by Early and Late Cretaceous subaerial
and marine arc-related volcano-sedimentary assemblages.
Mesozoic stratigraphy at the paleocontinental margin of Mexico (Oaxaquia and
Mixteca Terranes) is formed by Triassic submarine fan turbidites accreted during
Early Jurassic time; Middle Jurassic–evolved volcanic arc rocks are unconformably
covered by a Late Jurassic to Cretaceous calcareous platform.
Six stages in the tectonic evolution are proposed on the basis of the stratigraphic
and deformational events recorded in western Mexico: (1) A passive or rifting margin
developed along the western margin of continental Mexico throughout the Triassic. A
*[email protected]
Centeno-García, E., Guerrero-Suastegui, M., and Talavera-Mendoza, O., 2008, The Guerrero Composite Terrane of western Mexico: Collision and subsequent
rifting in a supra-subduction zone, in Draut, A., Clift, P.D., and Scholl, D.W., eds., Formation and Applications of the Sedimentary Record in Arc Collision Zones:
Geological Society of America Special Paper 436, p. 279–308, doi: 10.1130/2008.2436(13). For permission to copy, contact [email protected]. ©2008 The
Geological Society of America. All rights reserved.
279
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Centeno-García et al.
thick siliciclastic turbiditic succession of the Potosi Submarine Fan was accumulated
on the paleo-continental shelf-slope and extended to the west in a marginal oceanic
basin. (2) Subduction began in the Early Jurassic, and the turbidites of the Potosi
Fan with slivers of the oceanic crust were accreted, forming a wide subduction prism.
(3) Exhumation of the accretionary prism and development of a Middle Jurassic continental arc onto the paleo-continental margin (Oaxaquia and Mixteca Terrane) took
place, and also in the Zihuatanejo Terrane. (4) Intra-arc strike-slip faulting and rifting of the Middle Jurassic continental arc took place along with migration of the
subduction toward the west and development of a calcareous platform in Oaxaquia
and the Mixteca Terrane (continental Mexico). (5) Drifting of the previously accreted
Tahue and Zihuatanejo Terranes formed a series of marginal arc-backarc systems,
or one continuously drifting arc with intra-arc and backarc basins during Early to
middle Cretaceous time. (6) Deformation of the arc assemblages, and development of
Santonian to Maastrichtian foreland and other basins, date the final amalgamation of
the Guerrero Composite Terrane with the continental margin.
Keywords: Guerrero Terrane, Mexico, tectonics, Triassic subduction complex, Cretaceous arc volcanism.
INTRODUCTION
The present configuration of continental Mexico was built
after accretion of basement remnants and oceanic terranes. During most of their Mesozoic history, Proterozoic to Paleozoic
accreted terranes formed a relatively narrow neck of land adjacent to the North American craton. This was bordered on its
eastern side by rifting and on its western side by active subduction. Thus Mexico is probably one of the most suitable regions
in North America for studying the interaction between these two
differing tectonic scenarios. We suggest in this paper, based on
evidence recorded in the stratigraphy of the Guerrero Composite
Terrane and surrounding terranes, that the almost continuously
subducting Pacific margin of Mexico was directly influenced by
extensional tectonics associated with the breakup of Pangea and
the formation of the Gulf of Mexico.
The Guerrero Composite Terrane (Campa and Coney, 1983)
constitutes approximately one-third of Mexico. As originally
described, it is the largest of all the Mexican terranes and probably
the second largest of the North America Cordillera after Wrangellia (Campa and Coney, 1983; Centeno-García et al., 1993a). The
Guerrero Composite Terrane is characterized mostly by submarine and locally subaerial volcanic and sedimentary successions
that range in age from Jurassic (Tithonian) to middle–Late Cretaceous (Cenomanian), and scarce exposures of older rocks. A wide
variety of models has been proposed for the origin of the Guerrero
Composite Terrane. Like other terranes of the North America Cordillera, it was first interpreted as an exotic terrane formed by a fartraveled Cretaceous oceanic arc. Some authors have suggested that
it was an oceanic arc terrane that was accreted to nuclear Mexico
in Late Cretaceous time via a westward-dipping subduction zone
that closed a major ocean basin (Lapierre et. al., 1992; Tardy et
al., 1994; Dickinson and Lawton, 2001, etc.). Other authors have
suggested that the Guerrero Composite Terrane might represent
one or more complex systems of two or three peripheral arcs that
developed relatively close to the continent (Campa and Ramírez,
1979; Ramírez-Espinosa et al., 1991; Mendoza and Suastegui,
2000; Centeno-García et al., 2003; Centeno-García, 2005). Some
models even proposed that the arc was autochthonous and was
built upon Proterozoic continental crust of nuclear Mexico (de
Cserna, 1978; Elías-Herrera and Sánchez-Zavala, 1990). In other
words, there is a model for each likely possibility, but each lacks
strong supporting evidence.
New findings on the stratigraphy, discussed in this paper,
suggest a more complex evolution, implying a series of accretions to the continent followed by rifting, and later by collision.
In this paper we attempt to present our insights into the evolution of western Mexico gained from examining the stratigraphy
and structure, and the geochemical and geochronological data, of
such a vast area. However, we discuss in this paper only stratigraphic units and localities that are keys for reconstructing the
tectonic evolution. This paper synthesizes the work done by
many authors. Although there is the need for more geochronological and detailed field work, we consider that the preliminary
tectonic model presented in this paper is consistent with the evidence collected to date.
OVERVIEW OF THE GUERRERO COMPOSITE AND
NEIGHBORING TERRANES
The stratigraphy of western Mexico is synthesized in this
paper under the framework of tectono-stratigraphic terranes,
which are regions that share the same geological history and
are bounded by major faults. As mentioned before, by the early
Mesozoic, the Paleozoic and Proterozoic terranes were already
accreted to the southern part of the North American craton.
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Guerrero Composite Terrane of western Mexico
Those that already formed part of the continental margin during the Mesozoic were Oaxaquia and the Mixteca, Parral, and
Cortes Terranes (Fig. 1). Terranes accreted or displaced during
the Mesozoic were those of the Guerrero Composite, the Central,
as well as terranes of the western Baja California Peninsula. The
latter will not be reviewed in this paper. A brief summary of the
stratigraphy is described as follows; more detailed descriptions of
key areas and events are discussed later.
al., 1995; Ramírez-Ramírez, 1992; Lawlor et al., 1999; Solari
et al., 2003; Keppie et al., 2003). It is covered by Paleozoic
sedimentary rocks (Fig. 2) that are capped by Permian volcanic and volcaniclastic rocks (McKee et al., 1999; Stewart et al.,
1999; Rosales-Lagarde et al., 2005). Triassic (Carnian–Norian)
sedimentary rocks (La Ballena Formation) are exposed at the
western margin of Oaxaquia (Labarthe et al., 1982; SilvaRomo, 1993; Tristán-Gonzalez and Torres-Hernández, 1994;
Centeno-García and Silva-Romo, 1997; Barboza-Gudiño et al.,
1998, 1999, 2004; Bartolini et al., 2002). These rocks are made
up of a thick succession of turbidites (Fig. 2) deposited in a
submarine fan environment named the Potosi Fan (CentenoGarcía, 2005).
Triassic rocks of the Potosi Fan were deformed prior to deposition of Jurassic volcanic-volcaniclastic rocks (Centeno-García and
Silva-Romo, 1997). They are interpreted as a Jurassic continental
arc and rest unconformably on the Triassic Potosi Fan. Jurassic
arc strata are made up of subaerial andesitic-rhyolitic lava flows,
interbedded with volcaniclastic rocks (Silva-Romo, 1993). The
arc sequence changes transitionally upsection to shallow-marine
OAXAQUIA
At the end of the Paleozoic, Proterozoic basement terranes
of Gondwanan affinity were already accreted to the southern part
of the North American craton. The largest of these is the Oaxaquia block (Fig. 1), a crustal fragment, subcontinent in size, of
Grenville affinity (Ortega-Gutiérrez et al., 1995). This crustal
block forms the backbone of eastern Mexico and is referred to
herein as continental Mexico for the Mesozoic. Oaxaquia has
a Precambrian (1157–900 Ma) crystalline basement (gneisses
and anorthosites; Patchett and Ruíz, 1987; Ortega-Gutiérrez et
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Figure 1. Map showing main tectono-stratigraphic terranes, major faults mentioned in the text, and locations of Figures 4, 6, and 8.
282
Maastrichtian
Campanian
Coast Huetamo Northern
Caborca
Oaxaquia
Central
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Parral
Mixteca
Tahue
Guanajuato
Zihuatanejo
Teloloapan
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GUERRERO COMPOSITE TERRANE
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submarine volcanism
andesitic
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Cenomanian
Albian
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volcaniclastic rocks
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terrestrial and shallow
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Valanginian
Berriasian
Tithonian
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Sinemurian
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Rhaetian
Norian
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Ladinian
Early Triassic
Paleozoic
Proterozoic
Figure 2. Simplified stratigraphic columns for Oaxaquia and terranes mentioned in the text. They show the age range (in Ma) of sedimentation
and magmatism for western and central Mexico. Geochronological data are represented as follows: Black circles are U/Pb ages, and diamonds
are Ar/Ar and K/Ar ages.
volcaniclastic rocks, limestone, and some evaporites (Fig. 2;
Silva-Romo, 1993; Tristán-González and Torres-Hernández,
1994; Barboza-Gudiño et al., 2004). Calcareous sedimentation
in Oaxaquia ranges in age from late Oxfordian–Kimmeridgian to
Turonian and is interpreted as the southern extension of the North
American seaway. A major change upsection from calcareous to
clastic sedimentation occurred at the uppermost part of the Cretaceous, forming a thick succession of sandstone, shale, and conglomerate (Caracol Formation; Silva-Romo, 1993). Oaxaquia is
overthrust by the Guerrero Composite Terrane (Fig. 1).
MIXTECA TERRANE
The basement of the eastern Mixteca Terrane is made up of
pre-Mississippian polydeformed metamorphic rocks of the Acatlán Complex (Ortega-Gutiérrez, 1981; Ruíz et al., 1988; Yañez et
al., 1991). This complex is considered to be the result of complex
interactions between Gondwana and Laurentia previous and during the assembling of Pangea (Ortega-Gutiérrez et al., 1999). It
is unconformably overlain by Permian sedimentary rocks, which
are in turn overlain unconformably by Middle Jurassic volcanic
and sedimentary rocks (Fig. 2; García-Díaz et al., 2004). At the
western part of the terrane, near the limit with the Guerrero Composite Terrane, partly metamorphosed volcanic and volcaniclastic
rocks are exposed (Taxco Schist and Chapolapa Formation; de
Cserna and Fries, 1981; Talavera-Mendoza, 1993; Campa and Iriondo, 2004). The Taxco Schist is made up of andesitic to rhyolitic
lavas and volcaniclastic rocks of Early Cretaceous age (TalaveraMendoza, 1993; Campa and Iriondo, 2004). The Taxco Schist
is unconformably overlain by a thick limestone succession of
Albian to Cenomanian age and by Turonian–Maastrichtian clastic
rocks (Mexcala Formation; Campa and Ramírez, 1979; TalaveraMendoza et al., 1995). Contacts between the Mixteca Terrane and
Oaxaquia, as well as between the Mixteca and Guerrero Composite Terranes, are partially exposed. The Mixteca Terrane is on
strike-slip fault contact with Oaxaquia, and rocks of the Guerrero
Composite Terrane are thrust over the Mixteca Terrane.
PARRAL TERRANE
The Parral Terrane (Figs. 1 and 2) was first defined by
Pacheco et al. (1984) and Coney and Campa (1987) and was redefined by Centeno-García (2005). The basement of the Parral Terrane is formed by Devonian to Carboniferous metamorphic rocks
(Pescadito Schist; Eguiluz and Campa, 1982; Araujo and Arenas,
1986; Zaldivar and Garduño, 1984). These Paleozoic metamorphic rocks are unconformably overlain by red beds and volcanic successions (Nazas Formation; Pantoja-Alor, 1963), which
change transitionally to Tithonian limestone (Araujo and Arenas,
1986; Contreras-Montero et al., 1988). Cretaceous calcareous
and clastic sedimentation of the Parral Terrane is laterally continuous with the calcareous-clastic deposits that cover Oaxaquia
and the Central Terrane. Relationships among the Parral, Central, and Cortes Terranes and the Parral Terrane and Oaxaquia are
unknown, because the contacts are covered by Cretaceous limestone or by Cenozoic volcanic successions. Therefore, the exact
locations of their boundaries are unknown but are inferred by the
difference in styles of deformation of the Cretaceous rocks.
283
Paleozoic “miogeosyncline” of Nevada. It was transferred toward
the south by Middle to Late Jurassic time via the Mohave-Sonora
megashear (Anderson and Silver, 1979, 2005; Stewart et al.,
1990). The Cortes Terrane is interpreted as an autochthonous terrane to North America, which probably evolved at the margin of
the Caborca Terrane (Stewart et al., 1990). It is made up of a thick
succession of Paleozoic deep-marine turbidites that were thrust
over platform limestone of the Caborca Terrane (Figs. 1 and 2).
The Cortes Terrane is interpreted as continental-slope deposits, and it is considered the southern extension of the Paleozoic
Cordilleran “eugeoclinal” deposits from Nevada and California
(Poole and Madrid, 1988; Coney and Campa, 1987; Stewart et al.,
1990). The previously deformed Paleozoic deep-marine rocks of
the Cortes Terrane are overlain by Triassic (Carnian–Norian) terrestrial and marine sedimentary rocks (Stewart et al., 1990; Stewart and Roldán-Quintana, 1991). The Triassic rocks are overlain
by Cretaceous red beds and volcanic rocks (Stewart and RoldánQuintana, 1991). Contact relationships between the Cortes and
Guerrero Composite Terranes have not been well constrained,
but the contact is inferred to be a Late Cretaceous thrust fault.
CENTRAL TERRANE
The nature of the basement of the Central Terrane is unknown,
but it is assumed to be different from the Proterozoic basement of
Oaxaquia because its oldest exposed rocks near its contact are
a subduction-related accretionary complex (Taray Formation;
Anderson et al., 1990; Diaz-Salgado et al., 2003; Anderson et al.,
2005; Centeno-García, 2005). The subduction zone on which the
Taray Formation was deformed was probably constructed along
the Oaxaquia continental margin between Late Permian and Early
Jurassic time (Diaz-Salgado et al., 2003; Anderson et al., 2005).
The complex is unconformably overlain by Oxfordian subaerial
rhyolitic to andesitic volcanic rocks and red beds (Jones et al.,
1995). These rocks change transitionally to shallow-marine limestone that ranges in age from Late Jurassic to Late Cretaceous
(Córdoba-Méndez, 1964). The location of the northern and eastern contact between the Central Terrane and Oaxaquia is inferred
on the basis of the location of the last exposures of Paleozoic–
early Mesozoic rocks, and a contrast in deformation styles of Cretaceous rocks in both (Fig. 1). The contact between the Central
and Guerrero Composite Terranes has not been studied in detail
but is inferred on the basis of the distribution of the northernmost
exposures of Cretaceous marine volcanic rocks that belong to the
Guerrero Composite Terrane. Structural trends on both sides of
the contact suggest that the Central Terrane is overthrust by the
Guerrero Composite Terrane to the south (Fig. 1). The thrusting is
inferred to have occurred about Late Cretaceous time.
CABORCA AND CORTES TERRANES
The Caborca Terrane has a Proterozoic basement older than
1.7 Ga (Anderson and Silver, 1981), covered by a thick Paleozoic
sedimentary succession. It has been interpreted to be a displaced
block of continental North America, originally located along the
Areas with large volumes of Lower Cretaceous volcanic
and volcaniclastic rocks, located toward the west of Oaxaquia and the Mixteca Terrane, were originally grouped as the
284
Guerrero Terrane by Campa and Coney (1983) and were, 10
years later, divided into the Tahue, Nahuatl, and Tepehuano
Terranes by Sedlock et al. (1993). Subsequent regional mapping has shown that the divisions proposed by Campa and
Coney (1983) are closer to the field locations of faults delimiting the terranes than those of Sedlock et al. (1993). Therefore, more recent reviews of the terrane distribution of Mexico
(e.g., Centeno-García, 2005) have been based on Campa and
Coney (1983). The Guerrero is a composite terrane, formed by
at least five terranes: Tahue, Zihuatanejo, Guanajuato, Arcelia,
and Teloloapan (Figs. 1 and 2; Talavera-Mendoza et al., 1995;
Mendoza and Suastegui, 2000; Centeno-García et al., 2003;
Centeno-García, 2005). Their stratigraphy is briefly described
from NNW to ESE (Fig. 1):
Tahue Terrane
The Tahue Terrane contains the oldest rocks found so far
within the Guerrero Composite Terrane (Fig. 2; Centeno-García,
2005). These rocks comprise Ordovician marine rhyoliticandesitic lavas and clastic and calcareous rocks, all deformed
and metamorphosed to low-greenschist facies (El Fuerte Complex; Mullan, 1978; Roldán-Quintana et al., 1993; Poole and
Perry, 1998). These rocks may have originated as an oceanic
arc that apparently was accreted previous to the deposition of
Pennsylvanian–Permian deep-marine sedimentary rocks (San
José de Gracia Formation; Carrillo-Martínez, 1971; Gastil et
al., 1991; Arredondo-Guerrero and Centeno-García, 2003;
Centeno-García, 2005). These deep-marine turbidites are strongly
deformed but do not show the metamorphism of the El Fuerte
Complex; thus an unconformable contact relationship between
these two units is inferred. Paleozoic rocks of the Tahue Terrane
are unconformably overlain by Cretaceous marine arc volcanic
rocks and are interpreted as part of the Guerrero Arc (OrtegaGutiérrez et al., 1979; Henry and Fredrikson, 1987; RoldánQuintana et al., 1993; Freydier et al., 1995). These rocks are also
cut by mafic and ultramafic intrusions that are part of the same
Cretaceous arc magmatism (Henry and Fredrikson, 1987; Gastil et al., 1999; Arredondo-Guerrero and Centeno-García, 2003).
Therefore, the Paleozoic units form the basement upon which
the arc was built. The Tahue Terrane also contains metamorphic
rocks of Triassic age (Keppie et al., 2006). The contact relationship between the Cortes and Tahue Terranes has not been studied
in detail, but it is inferred to be a thrust (Fig. 1; Roldán-Quintana
et al., 1993). The contact between the Tahue and Zihuatanejo Terranes is not exposed.
Zihuatanejo Terrane
The Zihuatanejo Terrane is the largest of all terranes that
form the Guerrero Composite Terrane (Fig. 1). It extends north
of the Mexican Volcanic Belt and along the Pacific Coast of Mexico (Centeno-García et al., 1993a, 1993b; Talavera-Mendoza et
al., 1995; Mendoza and Suastegui, 2000). Its basement is made
up of large volumes of Triassic (Norian) quartz-rich turbidites
(sandstone and shale) that are tectonically imbricated (Campa
et al., 1982; Centeno-García et al., 1993a, 1993b). The turbidites form a matrix within which are blocks and slabs of pillow
basalts, diabase, banded gabbros, chert, and limestone (Fig. 2).
These rocks have received different names at different outcrops:
Zacatecas Formation, Arteaga Complex, and Las Ollas Complex
(Burckhardt and Scalia, 1906; Ranson et al., 1982; Cuevas-Pérez,
1983; Monod and Calvet, 1991; Centeno-García and SilvaRomo, 1997; Talavera-Mendoza, 2000; Centeno-García et al.,
2003). The deformation of these rocks varies from gently folded
strata to highly sheared block-in-matrix textures, and their metamorphism ranges from none to high-greenschist–amphibolite
facies (Centeno-García et al., 2003). Blueschist facies have been
reported only in one locality (Las Ollas Complex; TalaveraMendoza, 2000). These lithologies are interpreted to constitute
an Upper Triassic(?)–Lower Jurassic subduction-related accretionary complex.
Scattered exposures of rocks of Middle to Late Jurassic–
evolved arc volcanism lie along the Pacific Coast of the Zihuatanejo Terrane. These rocks are made up of submarine rhyolitic lavas and volcaniclastic rocks, and granitoids that were
emplaced in rocks of the accretionary complex (Bissig et al.,
2003; Centeno-García et al., 2003). The Middle to Upper Jurassic arc rocks were in turn deformed and exhumed previous to the
deposition of uppermost Jurassic–Cretaceous arc-related strata
(Centeno-García et al., 2003).
The Cretaceous arc succession ranges from Berriasian to
Cenomanian in age, and it includes andesitic, basaltic, and some
rhyolitic volcanic and volcaniclastic rocks, interbedded with
limestone, evaporites, and some red beds (Grajales and López,
1984). The arc succession contains abundant fossils such as rudists, gastropods, microfossils, fossil logs, and vertebrates.
This arc succession was deformed prior to the intrusion of
large granitoids of latest Cretaceous to Paleogene age (Schaaf
et al., 2000). Also, uppermost Cretaceous (Santonian to Maastrichtian) red beds and volcanic rocks rest unconformably on all
previous units (Altamira Areyán, 2002; Benammi et al., 2005).
The contact between the Zihuatanejo Terrane and Oaxaquia is
exposed at its northern limit, where Cretaceous arc rocks of the
Zihuatanejo Terrane are thrust over shallow-marine limestone of
Oaxaquia. Its contact with the Arcelia and Guanajuato Terranes
is inferred to be an east-verging thrust, but it is covered by uppermost Cretaceous and Cenozoic red beds and volcanic rocks.
Guanajuato Terrane
The Guanajuato Terrane has been interpreted as a complete crustal section through a primitive island arc that appears
to lack an older basement (Ortiz-Hernandez et al., 1991; OrtizHernandez, 1992). It has also been interpreted as the remains of
an oceanic basin that lay between the Guerrero arc and the continental margin (Freydier et al., 2000). This terrane was formed by
a series of tectonic slivers that placed lower crust rocks (gabbro,
tonalite, serpentinite, wehrlite, and dike swarms) on pillow
basalts, rhyolitic tuffs, volcanic turbidites, chert, and black detrital limestone (Quintero-Legorreta, 1992; Ortiz-Hernandez et al.,
1992; Lapierre et al., 1992; Monod et al., 1990; Martínez-Reyes,
1992; Ortiz-Hernandez et al., 2003). These rocks were poorly
dated as Tithonian–Hauterivian in age (Ortiz-Hernandez et al.,
2003; Hall and Mortensen, 2003). Previously deformed volcanic turbidites are unconformably overlain by Aptian–Albian
limestone (Ortiz-Hernandez et al., 2003). This suggests that
sedimentation and at least one phase of deformation occurred
previous to the Aptian–Albian (Ortiz-Hernandez et al., 2003).
At present the Guanajuato Terrane is thrust over the calcareous
platform of Oaxaquia (Ortiz-Hernández et al., 2002). Contact
relationships between the Guanajuato and Zihuatanejo Terranes
have not been constrained.
Arcelia Terrane
The Arcelia Terrane is made up of basaltic pillow lavas and
ultramafic bodies, black shale and chert, and volcanic turbidites,
all intensively deformed and partly metamorphosed (RamírezEspinosa et al., 1991; Talavera-Mendoza et al., 1995). It is characterized by Early Cretaceous deep-marine primitive arc or arcrelated oceanic facies and shows the least evolved magmatism
of all the arc successions of the Guerrero Composite Terrane
(Talavera-Mendoza et al., 1995; Mendoza and Suastegui, 2000).
The Arcelia Terrane appears to lack an older basement (TalaveraMendoza et al., 1995; Mendoza and Suastegui, 2000). Rocks of
the Arcelia Terrane apparently were thrust over the assemblages
of the Teloloapan Terrane, and were in turn overthrust by rocks
of the Zihuatanejo Terrane. However, these contacts are inferred
because they are covered by younger red beds.
Teloloapan Terrane
The Teloloapan Terrane consists of two distinct regions: the
eastern region is characterized by shallow-marine volcanic and
sedimentary deposits (Fig. 2), and the western region by deeper
volcanic and sedimentary facies (Guerrero-Suastegui et al., 1991;
Ramírez-Espinoza et al., 1991; Talavera-Mendoza et al., 1995;
Mendoza and Suastegui, 2000; Guerrero-Suastegui, 2004). Both
are marine arc assemblages, which vary in composition from
basalt-andesite to scarce dacite-rhyolite (Talavera-Mendoza
et al., 1995). This unit contains microfossils (radiolarians and
coccoliths), gastropods, and bivalves that range in age from
Hauterivian to Aptian; these rocks change transitionally upsection to Aptian–Albian island-arc carbonates (Guerrero-Suastegui
et al., 1991; Ramírez-Espinoza et al., 1991; Talavera-Mendoza et
al., 1995). The Teloloapan Terrane (Fig. 1) is exposed in the easternmost parts of the Guerrero Composite Terrane. It is characterized structurally by a complex thrust-fault system that verges
eastward. Its Lower Cretaceous rocks are severely deformed and
metamorphosed in low-grade greenschist facies. The Teloloapan
Terrane overrides either Lower to Middle Cretaceous platform
285
carbonates or Upper Cretaceous clastic sediments that belong
to the Mixteca Terrane (Fig. 1; Campa and Ramirez, 1979). The
nature of its basement remains unknown. Metamorphic rocks
that are exposed near the northwestern boundary of the Teloloapan Terrane with the Arcelia Terrane have been interpreted as a
possible basement for the former (Elías-Herrera and SánchezZavala, 1990; Sanchez-Zavala, 1993). The rocks in this area are
of uncertain age and origin.
TECTONIC MODEL
The most abundant rocks of the Guerrero Composite Terrane
are marine, and rarely subaerial, arc volcanic and sedimentary
successions that range in age from latest Jurassic (Tithonian) to
middle Late Cretaceous (Cenomanian). The composition of the
few scattered exposures of older units suggests a complex earlier
tectonic evolution. These older rocks were not taken into consideration for the tectonic models proposed by previous authors
(de Cserna, 1978; Campa and Ramirez, 1979; Elías-Herrera and
Sánchez-Zavala, 1990; Tardy et al., 1994; Lapierre, et. al., 1992;
Dickinson and Lawton, 2001, etc.). Based on the available information, we identified six main tectonic stages in the evolution of
the Guerrero Composite Terrane. These stages are represented in
Figure 3 and are briefly described in this section. Detailed discussion of the data that support the reconstruction of each stage is
presented in the following section.
Stage I: Collision of a Paleozoic Oceanic Arc?—Basement
of the Tahue Terrane
The basement of the Tahue Terrane (Fig. 3) is composed of
the early Paleozoic accreted volcanic-sedimentary rocks of the
El Fuerte Metamorphic Complex. There are not enough data
available to constrain the origin of this complex. Preliminary
interpretations considered these rocks as remnants of Gondwanan crust accreted during the formation of Pangea (Poole et al.,
2005). In this model, metamorphic rocks of El Fuerte could be
the western continuation of basement rocks of the Parral Terrane
(Figs. 1 and 2). An alternative interpretation is that the El Fuerte
Complex may be a displaced fragment of the early Paleozoic arc
(Antler Arc) that collided with the western continental margin of
North America during late Paleozoic time (Burchfiel et al., 1992;
Sánchez-Zavala et al., 1999; Dickinson, 2004; Centeno-García,
2005). Carboniferous deep-marine turbidites (San José de Gracia
Formation) that apparently cover the lower Paleozoic arc rocks
unconformably may be correlative with deep-marine sedimentary rocks exposed in the eastern peninsular ranges of Baja California and the southwestern Cordillera of North America (Gastil
et al., 1991; Centeno-García, 2005).
In either of the two scenarios, deformed Paleozoic rocks of
the Tahue Terrane are the basement upon which Cretaceous volcanism was built, indicating an earlier history of accretion of the
Guerrero Composite Terrane than was previously interpreted by
other authors.
W
Tahue
(Guerrero Composite Terrane)
Passive margin sediments
E
Cortes
Stage I
Arc collision and
development of a passive
margin
Caborca
Paleozoic
Vizcaíno?
Zihuatanejo (Guerrero Composite)
and Central terranes
Oaxaquia
Continent margin
Siliciclastic turbidites share the same provenance
Stage II
Marginal oceanic basin
with active rift volcanism
n
Potosí Submarine Fan
Vizcaino?
Oaxaquia and Mixteca
Arteaga Basin
Triassic
Carnian-Norian
Vizcaíno?
Guerrero
Central
Oaxaquia
Potosi Fan
(deformed)
Taray Complex
Arteaga Complex
Stage III
Accretion via subduction
wide accretionary prism
?
?
Early Jurassic
pre 180-163 Ma
Guerrero
Central
Oaxaquia
transtension?
Tumbiscatío
Granitoid
163-158 Ma
158 Ma
?
+Oaxaquia and Mixteca
Sub
+
Stage IV
Continental arc and
contemporaneous strike-slip
and extension (roll-back of
the subducting plate?)
Middle to
Late Jurassic
duc
Guerrero
Zihuatanejo/Tahue
Composite Terrane
Arcelia
Guanajuato
Teloloapan
tion
Central
and Mixteca
Oaxaquia (north)
transtension?
Calcareous K platform
?
Sub
?
?
Stage V
Formation of a multiple arcs
system or a single arc with
intra-arc/back arc rifting
Cretaceous
Berriasian-Cenomanian
duc
tion
Guerrero
Zihuatanejo/Tahue
Composite Terrane
Arcelia
Teloloapan
Guanajuato
Central / Oaxaquia
and Mixteca (south)
compression
granitoids 105 Ma
Red Beds
Marine turbidites
Stage VI a
Deformation and locally
metamorphism, cut by
105 Ma granitoids in the
Zihuatanejo terrane
Cretaceous
Cenomanian?-pre Santonian
Stage VI b
Active continental arc in
the west and syntectonic
marine turbidites (foreland)
in the east and deformation
Cretaceous
Santonian?-Maastrichtian
Figure 3. Tectonic models for the evolution of western Mexico, showing the alternating stages of subduction-collision and rifting.
Stage II: Late Triassic Passive Margin—Deposition of the
Potosi Fan
The paleo-continental edge of Mexico lay approximately
at the western boundary of the Oaxaquia and Mixteca Terranes
in the early Mesozoic (Fig. 1; Centeno-García, 2005). Thus the
Central and Guerrero Composite Terranes (Fig. 1) were accreted
or displaced to their present position during the Mesozoic. Sedimentation along the western continental margin of Oaxaquia was
dominated by large volumes of siliciclastic turbidites (quartz-rich
sandstone and shale) that were deposited in the distal continental
shelf or at the continental slope at least during Carnian–Norian
time (Fig. 3). Accretionary complexes that form the basement of
the Central Terrane and parts of the Guerrero Composite Terrane
(Zihuatanejo Terrane) are formed largely (up to 60% of the total
area of exposures) by similar quartz-rich sandstone and shale
turbidites that made up the matrix within which blocks of variable composition are embedded. These turbidites in the accreted
terranes contain fossils of the same age as those from turbidites
deposited at the continental slope of Oaxaquia.
Detrital zircon ages obtained from turbidites from all the
localities of the Carnian–Norian turbidites, from Oaxaquia to
basal accretionary complexes of the Central and Zihuatanejo Terranes, show the same populations, which suggest that the fan turbidites spread into a marginal oceanic basin that was later accreted
to the continental margin. These siliciclastic rocks are grouped as
the Potosi Fan (Centeno-García, 2005) and are important because
they can be traced from Oaxaquia to the present Pacific Coast
of Mexico, and they tie together the Central Terrane, the westernmost part of the Guerrero Composite Terrane (Zihuatanejo
Terrane), and the continental margin of southern North America
(Oaxaquia) during Late Triassic time. Thus, the Potosi Submarine Fan may have been a large sedimentary feature, probably
close to the dimensions of the present Bengal Fan.
There is no evidence of Triassic magmatism in continental
Mexico, and detrital zircon geochronology of the fan turbidites
show that the youngest age populations are much older than depositional ages in all the studied localities of the Potosi Fan (Fig. 3;
Centeno-García et al., 2005; Centeno-García, 2005). Therefore,
the Potosi Fan probably was deposited across a passive margin,
or at least a margin that had no active subduction along the length
of the fan at the time of deposition.
Stage III: Accretion of the Potosi Fan to the Continental
Margin via Subduction—Basement of the Central and
Zihuatanejo Terranes
All the Triassic units of central and western Mexico are
strongly deformed and partially metamorphosed, indicating that a
major compressional event occurred during latest Triassic–Early
Jurassic time. This event is characterized by tight folding, shearing, and axial cleavage in the continent-slope deposits of the
Potosi Fan in Oaxaquia (La Ballena Formation), and blockin-matrix texture in the Taray Formation (Central Terrane),
287
in the Zacatecas Formation, and in the Arteaga and Las Ollas
Complexes (Zihuatanejo Terrane). These last three units formed
in the distal ocean-floor zone of the Potosi Fan. The presence
of mélanges (Arteaga Complex and Taray Formation) as well as
blueschist in the Las Ollas Complex (Zihuatanejo Terrane) indicates that deformation occurred in a subduction zone. During this
deformational event the turbidites of the Potosi Submarine Fan,
with slivers of the oceanic crust and its sedimentary cover, were
accreted to the continent. This accretionary prism apparently
was very wide, as suggested by the large areas that are floored
by it. Whether the subducting slab was dipping toward the west
(under an oceanic arc) or the east (under continental Mexico)
has not been constrained. There are two isolated reports of dated
Early Jurassic volcanic rocks in Oaxaquia (Barboza-Gudiño et
al., 2004; Fastovsky et al., 2005), but whether they are part of a
continental arc or not is not known. Evidence of contemporaneous oceanic-arc magmatism is exposed in the Vizcaíno Peninsula of Baja California (Kimbrough and Moore, 2003), where
Triassic–Jurassic volcanic rocks have geochemical signatures of
primitive arc affinity. It is possible that the rocks in the Vizcaíno
Peninsula represent a displaced fragment of an oceanic arc that
accreted to the Arteaga and Las Ollas Complexes of the western
Guerrero Composite Terrane, which in turn accreted to the Taray,
Zacatecas, and La Ballena Formations, but this model needs to be
supported by more evidence.
Stage IV: Late Jurassic Continental Arc—Overlapping
Assemblage for Guerrero Composite Terrane, Central
Terrane, Oaxaquia, and Mixteca Terrane
Subaerial volcanic and sedimentary rocks, as well as shallow
porphyritic intrusives, dikes, and sills, overlie or cut previously
deformed Triassic sedimentary rocks in Oaxaquia and rocks of
the accretionary prism in the Central Terrane. These rocks range
in age from 174 to 158 Ma (Jones et al., 1995; Barboza-Gudiño
et al., 2004). A common attribute of all the outcrops of these
rocks is that they are mostly rhyolitic in composition, with minor
dacitic-andesitic lava flows and tuffs, and show evolved-arc geochemical signatures (Centeno-García and Silva-Romo, 1997;
Centeno-García, 2002; Centeno-García and Díaz-Salgado, 2002).
Coeval volcanic rocks have been reported in the Mixteca Terrane
as well, suggesting that arc volcanism was widespread in continental Mexico at that time (García-Díaz et al., 2004). Rocks of
similar age range and similar evolved-arc geochemical signatures
are exposed in the western Zihuatanejo Terrane of the Guerrero
Composite Terrane (Bissig et al., 2003; Centeno-García et al.,
2003). This suggests that the Guerrero Composite Terrane may
have been incorporated into the continental margin by that time.
Summarizing the data described above: (1) Triassic basement rocks of the Zihuatanejo Terrane (Guerrero Composite Terrane) share a provenance linkage with rocks of the same age in
Oaxaquia and the Central Terrane; (2) all Triassic rocks, from
those deposited on the paleo-continent’s margin of Mexico to
those within the accreted terranes, were deformed previous to the
288
development of a Late Jurassic continental arc; and (3) evolved
Upper Jurassic continental-arc volcanism was widespread among
continental Mexico and accreted terranes (Central and Zihuatanejo Terranes). On the basis of these facts, we propose in this
paper that the first accretion of the Guerrero Terrane occurred
during latest Triassic–Early Jurassic time instead of near the
end of the Cretaceous, as previously proposed by other authors.
Therefore, the Late Jurassic magmatic event represents an overlapping assemblage that stitches all the terranes of central and
western Mexico for that period.
Stage V: Late Jurassic–Early Cretaceous Intra-Arc Strike
Slip(?)–Rifting of the Continental Arc—Drifting of the
Guerrero Composite Terrane
It has been proposed that major lateral displacements
occurred during the activity of the Jurassic continental arc of
stage IV (Anderson and Silver, 2005). Therefore, the arc was
originally in a more northerly position, and it was displaced, via
the Mojave-Sonora Megashear, to its present position in central
Mexico prior to, or at, the early stage of development of the calcareous platform (Anderson and Silver, 2005).
Whether this major strike-slip system existed or not has been
widely discussed (see GSA Special Paper 393). We consider that
extensive geological evidence of major tectonism during and
after arc volcanism exists (see following discussion). The cessation of magmatism in the Central Terrane and Oaxaquia suggests
a change in the location of the subduction zone. Then, a major
regional calcareous platform developed over the arc and other
older rocks. This major transgression initiated the deposition
of limestone on Oaxaquia, and on the Mixteca and Central Terranes. Calcareous sedimentation in central and eastern Mexico
was characterized by high subsidence rates (Goldhammer, 1999).
Arc magmatism continued only in a small area in the western
Mixteca Terrane and became widespread in the Guerrero Composite Terrane. Although there is some overlap in age ranges of
arc volcanism among the terranes that form the Guerrero Composite Terrane, there is a general trend from older ages in eastern
Oaxaquia and the Central Terrane to younger ages in the western
Guerrero Composite Terrane (Fig. 3). This suggests a possible
W-SW migration of the subduction zone. We propose that during and after the continental arc activity (Late Jurassic–Early
Cretaceous time), large amounts of extension and lateral translations may have occurred (see inferred faults in Fig. 1). This
extensional-transtensional(?) event split the continental arc, initiating the drifting of parts of previously accreted oceanic rocks
(basements of the Tahue and Zihuatanejo Terranes) and the generation of new oceanic crust (Guanajuato and Arcelia Terranes).
With the data available, it seems that volcanic activity at the
northern Zihuatanejo Terrane and at the Guanajuato and Teloloapan Terranes was restricted to latest Jurassic–Early Cretaceous
time (Fig. 3). In contrast, in the Arcelia, Tahue, and southern
Zihuatanejo Terranes, arc volcanism apparently continued up
to Albian–Cenomanian time (Fig. 3). Geochemical and isotopic
compositions of most of the Upper Jurassic–Cretaceous igneous
rocks of the different arc assemblages of the Guerrero Composite
Terrane suggest primitive sources, with little or no influence on
an evolved continental crust (e.g., Ortiz-Hernandez et al., 1991;
Lapierre et al., 1992; Centeno-García et al., 1993a; Freydier et al.,
1995; Gastil et al., 1999; Talavera-Mendoza et al., 1995; Mendoza and Suastegui, 2000, among others). Basalts with oceanisland (OI) and mid-oceanic-ridge basalt (MORB) signatures of
the Arcelia and Guanajuato terranes (Lapierre et al., 1992; OrtizHernandez et al., 2003; Mendoza and Suastegui, 2000) suggest
the influence of a mantle source for the magmatism.
Regional differences in the strata suggest abrupt lateral
changes in the depositional environments from shallow marine
to deep marine. Also, lateral differences in thickness of the successions suggest that they may have been deposited in alternate
subsiding basins and basement highs where the deposits draped
thinly or were absent. These major geological differences suggest
that intra-arc rifting was considerable and was probably associated with a complex paleogeography of marginal arc and backarc
systems in western Mexico. Whether or not the different terranes
of the Guerrero Composite Terrane were formed in a single arc
has not been constrained. Some authors proposed that the Guerrero Terrane formed from a complex system of two or three arcs
(Ramírez-Espinosa et al., 1991; Mendoza and Suastegui, 2000).
However, no Cretaceous subduction-related accretionary prisms
have been identified within any of the terranes of the Guerrero
Composite Terrane.
Stage VI: Final Accretion of the Guerrero Composite
Terrane, and Development of a New Continental Arc
A major Late Cretaceous–early Paleogene orogenic phase is
recorded throughout Mexico, coeval to the Sevier and Laramide
orogenies in western North America. This event is associated with
the Mexican Fold and Thrust Belt of the Sierra Madre Oriental.
Apparently, final amalgamation of the Guerrero Composite Terrane occurred during this orogenic event, and volcanic and sedimentary rocks of the Teloloapan, Guanajuato, Zihuatanejo, and
Tahue Terranes were thrust over the calcareous platform rocks
of Oaxaquia and the Central, Cortes, and Mixteca Terranes. The
amount of tectonic transport apparently is significant, as xenoliths of Precambrian continental crust were found in Cenozoic
volcanic rocks that erupted onto accreted rocks of the Guanajuato
Terrane (Urrutia-Fucugauchi and Uribe-Cifuentes, 1999). Significant tectonic transport is also suggested by the amount of
shortening that produced tight folding and major thrusting within
the northern Zihuatanejo Terrane and the Arcelia and Teloloapan
Terranes (Salinas-Prieto et al., 2000). In contrast, deformation of
Cretaceous rocks in the southern parts of the Zihuatanejo Terrane
formed wide regional anticlines, and some overturned folds and
minor thrust faults locally. The structures generally trend NWSE, although locally some structures trend N-S and E-W.
Santonian terrestrial sedimentation covers unconformably
the previously deformed arc assemblages of the Zihuatanejo
Terrane (Benammi et al., 2005). Synorogenic sedimentary basins
(Caracol Formation in Oaxaquia, and Mexcala Formation in the
Mixteca Terrane) containing clasts derived from the Guerrero
Composite Terrane suggest that these terranes were deformed
and exhumed by that time. In addition, synorogenic sedimentation overlaps the Arcelia and Teloloapan terranes (Miahuatepec
Formation), which suggests that these two terranes were also
amalgamated during the same orogenic event (Mendoza and Suastegui, 2000; Guerrero-Suastegui, 2004). All these synorogenic
basins range in age from Turonian to Maastrichtian. In addition,
Paleocene granitoids along the coast cut the previously folded
units of the Zihuatanejo Terrane and suggest a Late Cretaceous–
early Paleogene deformation.
Therefore, final amalgamation of the Guerrero Composite
Terrane occurred between Santonian and Turonian–Maastrichtian time.
DISCUSSION
This section summarizes the stratigraphic, structural, and
geochemical data that support the proposed stages for the tectonic evolution of western Mexico.
Stage I: Origin of the Basement of the Tahue Terrane
Exposures of pre-Cretaceous rocks in northwest Mexico
are scattered; thus contact relationships among them can only
be indirectly inferred (Figs. 1 and 4). Approximate distribution
of the contacts among the terranes of western Mexico (Caborca,
Cortes, and Tahue; Figs. 1 and 4) was outlined on the basis of
the geographic distribution of pre-Cretaceous outcrops and lateral changes in the isotopic signatures of Cretaceous–Paleogene
granitoids (Valencia-Moreno et al., 2001). Thus the nature of the
contacts and the amount of displacement among different basements are unknown. In this section the main stratigraphic units
that define the terranes are described following a NW to SE transect throughout the Paleozoic rocks of the Caborca, Cortes, and
Tahue Terranes (Guerrero Composite Terrane).
At the southern margin of the Caborca Terrane a thick shelfal limestone succession is exposed that contains Carboniferous–
Permian fusulinids and other shallow-marine fossil fauna (Stewart et al., 1990). These rocks are overridden by a north-verging
major thrust fault that places deeper marine sedimentary rocks
of the Cortes Terrane on the shelfal rocks of the Caborca Terrane (Fig. 1; Coney and Campa, 1987; Poole and Madrid, 1988;
Stewart et al., 1990).
Basal metamorphic rocks are not exposed in the Cortes Terrane, but its basement has been interpreted as thinned Proterozoic
rocks, perhaps the same as in the Caborca Terrane, or else Proterozoic metamorphic rocks different from those of the Caborca
Terrane (McDowell et al., 1999; Valencia-Moreno et al., 1999;
Valencia-Moreno et al., 2001). The deep-marine sedimentary
rocks of the Cortes Terrane are sandstone and shale turbidites,
graptolitic shale, chert, and layered barite that range in age from
289
Ordovician to Devonian–Early Mississippian and were deformed
during the Mississippian (Poole and Madrid, 1988; Stewart et al.,
1990). These rocks are in turn overlain by Upper Carboniferous
and Permian turbidites (Fig. 5; Poole and Madrid, 1988; Stewart et al., 1990; Poole et al., 2005). They all were deposited in
a deep-marine environment and are interpreted to be part of the
Paleozoic continental slope-rise deposits of western North America (Poole and Madrid, 1988; Stewart et al., 1990). All these units
of the Cortes Terrane were deformed and thrust over the Caborca
Terrane by Late Permian to Early Triassic time, and they are
unconformably covered by Upper Triassic terrestrial and marine
sedimentary rocks (Stewart et al., 1990). Therefore, the Caborca
and Cortes Terranes were assembled by early Mesozoic time.
The nature of the contact between the Cortes and Tahue Terranes (the latter belonging to the Guerrero Composite Terrane)
has not been mapped in detail. It is inferred to be a thrust that
verges toward the north, and it is probably north of El Fuerte
town in Sinaloa State (Fig. 5), based on the northernmost exposures of Cretaceous marine volcanic rocks of the Guerrero Terrane (Servais et al., 1982; Henry and Fredrikson, 1987; RoldánQuintana et al., 1993; Freydier et al., 1995).
The oldest Paleozoic rocks of the Tahue Terrane (Guerrero Composite Terrane) are exposed in the area of El Fuerte
(El Fuerte Complex; Figs. 4 and 5). The El Fuerte Complex is
formed by marine rhyolitic to andesitic lava flows and volcaniclastic rocks, interbedded with quartz-rich sandstone, shale,
and thin-bedded limestone (Mullan, 1978; Roldán-Quintana et
al., 1993; Poole and Perry, 1998). All these various components
are deformed and metamorphosed to greenschist facies (Mullan, 1978; Roldán-Quintana et al., 1993). Sedimentary rocks of
the El Fuerte Complex contain Ordovician conodonts (Poole
and Perry, 1998). Preliminary geochemical analyses indicate a
calc-alkaline island-arc affinity for the volcanic rocks of the El
Fuerte Complex, and are similar to those from coeval Paleozoic arc rocks in the Klamath Mountains of Northern California
(Lapierre et al., 1987). However, more detailed geochemical
and geochronological work needs to be done to constrain their
origin and relationships.
Upper Paleozoic deep-marine sedimentary rocks are exposed south of El Fuerte, in San José de Gracia town, Mazatlán City, and other scattered localities in Sinaloa State (Figs. 4
and 5). These rocks belong to the San José de Gracia Formation
(Carrillo-Martínez, 1971; Gastil et al., 1991; Arredondo-Guerrero
and Centeno-García, 2003) and are made up of quartz-rich sandstone and shale turbidites, thin-bedded calcareous debris flows,
black shale, and chert. The turbidites contain olistoliths of limestone with chert nodules, which in turn contain Middle Pennsylvanian to Early Permian fossils at the San José de Gracia locality
(Carrillo-Martínez, 1971; Gastil et al., 1991). The San José de
Gracia Formation has been interpreted as deposits in a deepmarine environment (Gastil et al., 1991). The contact between
the El Fuerte Complex and the San José de Gracia Formation
is not exposed. However, major differences in deformation and
metamorphism (turbidites of the San José de Gracia Formation
Hermosillo
e
a Terran
Caborc
e
n
a
rr
e
Cortes T
Ciudad
Obregón
S O N O R A
Navojoa
27°
Caborca Terrane
Limestone (Lower Cretaceous)
Shallow marine limestone
and shale (Paleozoic)
Cortes Terrane
Terrestrial and marine
sedimentary rocks (Triassic)
Deep Marine turbidites, chert
and barite (Paleozoic)
ne
rra e
e
s T rran
rte
Te
Co ue
h
a
T
Sonobari
El Fuerte
C
N
H
San Jose de Gracia
I
H
26°
U
A
H
Sinaloa de Leyva-Porohui
U
A
D
U
R
A
25°
N
Overlapping units
G
CULIACÁN
Recent sediments
O
Recent basalts
Miocene-Pliocene
Volcanic and sedimentary
(conglomerate-sandstone)
Granitoids (Paleocene-Oligocene)
Upper Cretaceous-Oligocene
Tarahumara Formation and Lower and Upper 24°
Volcanic Supergroup
Tahue Terrane (Guerrero Composite Terrane)
Granitoids (Upper Jurassic-Lower Cretaceous)
Cretaceous Guerrero Arc
Marine volcanic and sedimentary rocks
San Francisco Gneiss (Triassic)
23°
MAZATLÁN
San Jose de Gracia Fm. (Carboniferous)
El Fuerte Complex (Ordovician)
0
109°
108°
107°
25
50
100
km
106°
Figure 4. Geologic map of Sinaloa and the southern Sonora states, showing the geology of Caborca, Cortes, and Tahue Terranes (after
Carrillo-Martínez, 1971; Mullan, 1978; Gastil et al., 1978; Henry and Fredrikson, 1987; Stewart and Roldán-Quintana, 1991; Ortega et
al., 1992; and our own work).
metamorphosed
volcanic and quartz-rich
turbidites, limestone,
chert, basalts and rhyolites
El Fuerte Complex
Ordovician
migmatized gneisses
and amphibolites
Francisco gneiss
Upper Triassic
unconformity
dike swarm
linked by provenance (Potosí Fan)
?
matrix is quartz-rich turbidites
blocks of pillow lavas, chert,
serpentinite and limestone
accretionary complex
Taray Fm.
Paleozoic-Triassic?
unconformity
felsic lavas and
volcaniclastics
continental
Oxfordian
Transitional
from continental to
marine shale,
sandstone, evaporites,
limestone
Kimmeridgian-Tithonian
Limestone
Titonian to Aptian
Central Terrane
Hauterivian-Tithonian?
deep marine volcaniclastic
turbidites,chert, limestone
Arperos Fm.
unconformity
Albian-Aptian
massive limestone,
black limestone
shales and sanstone
La Luz
basaltic flows La Perlita
and tuff
limestone
limestone, chert,
volcaniclastic turbidites
felsic lavas 146 Ma
Esperanza Fm.
Tuna Mansa
diorite
Cerro Pelon
tonalite
Santa Ana
Guanajuato Terrane
blocks of pillow lavas
Zacatecas Fm.
Norian-Carnian
unconformity
150-147 Ma
felsic and
basic lavas
volcanic turbidites
calcareous debris flows,
tuff and chert
pillowed lavas and dikes
deformed and in part
metamorphosed
La Borda,
El Saucito and
ChilitosFms.
Lower Cretaceous
Aptian?
Zihuatanejo Terrane
volcanic turbidites
limestone, tuff and
chert, pillowed lavas
and dikes deformed
and in part
metamorphosed
Tahue Terrane
deformed quartz-rich
turbidites
continent-slope facies
La Ballena Fm.
Carnian-Norian
unconformity
Transitional
from continental to
marine shale,
sandstone, evaporites,
limestone
Oxfordian-Tithonian
felsic lavas and
continental
unknown age
Felsic lavas and
189-172 Ma
Limestone
Tithonian to Aptian
shale and sandstone
foreland-basin fill
western Oaxaquia
Caracol Fm.
EAST
Figure 5. Simplified stratigraphic columns for Oaxaquia and terranes north of the Transmexican Volcanic Belt. The columns are in an east-west order. They include the Tahue Terrane,
which is part of the Guerrero Composite Terrane. Vertical scale shows the age range (in Ma).
Paleozoic
Ladinian
Early Triassic
Carnian
Norian
Rhaetian
Hettangian
Sinemurian
Pliensbachian
Toarcian
Aalenian
Bathonian
Bajocian
Callovian
Oxfordian
Kimmeridgian
Tithonian
Berriasian
Valanginian
Hauterivian
Barremian
Aptian
Albian
Cenomanian
Turonian
Coniacian
Santonian
Campanian
Maastrichtian
WEST
292
are strongly deformed but not metamorphosed) indicate that the
contact is probably an angular unconformity.
Both units of the Tahue Terrane (El Fuerte Complex and
San José de Gracia Formation) are important because they can
constrain the paleogeography of the northern Guerrero Terrane.
Preliminary single-grain, detrital zircon geochronology from
the quartz-rich sandstone from the turbidites of the San José de
Gracia Formation shows populations that have a North American
affinity (Centeno-García et al., unpublished data) and are similar
to those from Paleozoic rocks in Baja California, in the Cortes
Terrane, and in Nevada (Gehrels et al., 2002).
The stratigraphy, geochemistry, and provenance of the Paleozoic rocks suggest that the Tahue Terrane (Guerrero Composite
Terrane) was linked to the tectonic evolution of the western continental margin of North America, probably up to Permian–Triassic
time. After that, there were major differences in the composition
of the Mesozoic sedimentary cover of the Caborca-Cortes Terranes with respect to that of the Tahue Terrane. Therefore, it is
likely that a fragment of previously accreted island-arc and continent-margin assemblages drifted from the continental margin
sometime in the early Mesozoic.
Contact relationships between the Paleozoic sedimentary
rocks of the San José de Gracia Formation (Tahue Terrane) and
the Triassic subduction-related complex of the Zihuatanejo Terrane are unknown because the contact is covered by younger
rocks. However, the Tahue and Zihuatanejo Terranes share similar Cretaceous volcanic and sedimentary cover.
Stages II and III: Triassic Potosi Fan and Its Accretion to
the Continental Margin
There are few exposures of Triassic rocks in Mexico, and
they are limited to the Caborca and Cortes Terranes, western
Oaxaquia, the Central and Zihuatanejo Terranes, and a small outcrop in the Vizcaíno Peninsula in Baja California. Triassic rocks
have not been found in the Mixteca Terrane or in other terranes
of Mexico. In this section we briefly describe Triassic rocks of
the Cortes and Tahue Terranes (Barranca Group and Francisco
Gneiss) and focus on the marine Triassic rocks of Oaxaquia (La
Ballena Formation), the Central Terrane (Taray Formation), and
the Guerrero Composite Terrane (Zacatecas Formation, and the
Arteaga and Las Ollas Complexes).
Barranca Group and Francisco Gneiss
Triassic (Carnian–Norian) sedimentary rocks of the Cortes
Terrane are made up of fluvial sandstone and shale that contain
abundant coal layers (Barranca Group; Stewart and RoldánQuintana, 1991). These sediments were deposited unconformably on previously deformed Paleozoic deep-marine rocks. The
Triassic fluvial deposits change transitionally up the column to
shallow-marine siliciclastic deposits. These rocks have no evidence of contemporaneous volcanism. In contrast, Triassic rocks
of the Tahue Terrane (Guerrero Composite Terrane) are made up
of metamorphosed igneous rocks of the Francisco Gneiss near
Sonobari (Figs. 4 and 5; Mullan, 1978; Keppie et al., 2006).
The Francisco Gneiss is made up of migmatized gneisses and
amphibolites that have within-plate and continental tholeiite geochemical signatures (Keppie et al., 2006). This suggests that the
Tahue and Cortes terranes may have been geographically separated by that time.
La Ballena Formation
Triassic rocks of Oaxaquia crop out on its western margin,
near its boundary with the Guerrero Composite Terrane (Figs. 1
and 6). They are grouped as the La Ballena Formation (SilvaRomo, 1993; Silva-Romo et al., 2000), and their largest exposures are in the Peñón Blanco, Charcas, and Real de Catorce
areas (Fig. 6; Silva-Romo, 1993; Tristán-González and TorresHernández, 1994; Barboza-Gudiño et al., 2004). The La Ballena
Formation is made up of quartz-rich sandstone and shale, and
scarce conglomerates deposited as small channel-fill lenses. The
sedimentary structures of these Triassic rocks indicate deposition mostly by turbidity currents, although some debris flows
and large slumps are present. This sequence contains abundant
trace fossils and ammonites and bivalves of Late Triassic (Carnian) age at the Peñón Blanco and Charcas areas (Cantu-Chapa,
1969; Silva-Romo et al., 2000; Bartolini et al., 2002). Sedimentary structures and fossil fauna suggest that the deposition of this
unit occurred in a submarine fan that developed on an external
platform or continental slope setting. These rocks form part of
the Potosi Submarine Fan (Centeno-García, 2005). The original thickness is unknown, but up to 4640 m was penetrated by
exploration drilling without reaching the base of the succession
(López-Infanzón, 1986).
Taray Formation
Similar marine siliciclastic rocks crop out at the Pico de
Teyra region in the Central Terrane (Figs. 5 and 6). They belong
to the Taray Formation, made up of highly deformed quartz-rich
turbidites (sandstone and shale) interbedded with some black
chert and scarce detrital limestone that contains fragments of crinoids, gastropods, corals, bivalves, and bryozoans (Diaz-Salgado
et al., 2003). The Taray siliciclastic turbidites form a matrix
within which blocks of black and green chert, pillow basalts, serpentinite, and crystallized limestone can be found (Figs. 5 and 6;
Diaz-Salgado et al., 2003). The age of this unit remains undetermined; however, there are reports of fusulinids from one of the
limestone blocks (Anderson et al., 1990). The youngest detrital
zircons collected from the sedimentary matrix are Late Permian
in age (Diaz-Salgado et al., 2003). There is also a report of molds
of bivalves of possible Carnian age (Barboza-Gudiño et al., 1999;
Bartolini et al., 2002). Thus deposition of the sedimentary matrix
should have occurred between the Late Permian to the Late Triassic. The Taray Formation has a block-in-matrix structural style,
formed by centimeter-size blocks to blocks of hundreds of meters
in size, all in a highly sheared sedimentary matrix. This characteristic is typical of a subduction accretionary complex (Anderson et al., 1990, 2005; Diaz-Salgado et al., 2003).
293
100°
101°
102°
Cenozoic cover
Caopas
U/Pb 158 Ma
Oaxaquia and Central Terrane
Concepción
del Oro
Pico
de
Teyra
Ju-K Calcareous Platform
Ju felsic and intermediate lava
flows, epiclastic rocks and redbeds
24°
Huiznopala
Granjeno
Central
terrane
Real de
Catorce
Matehuala
Huizachal
U/Pb190 Ma
Tr Quartz-rich shale and sandstone
turbidites (Potosí Fan)
Tr(?) Accretionary complex
blocks of pillow basalt, ultramafic,
chert, and marble in a sedimentary
quartz-rich matrix
Proterozoic and Paleozoic
metamorphic and sedimentary
rocks
Guanajuato Terrane
Ju-K pillow basalts, deep marine
volcanic turbidites, chert, and mafic
and ultramafic plutons
Charcas
23°
Zacatecas
U/Pb 147-150 Ma
Oaxaquia
Peñón
Blanco
San Luis Potosí
Zihuatanejo Terrane
Ju-K pillow basalts, volcanic
turbidites, detrital limestone
Tr Accretionary complex
blocks of pillow basalt, in a
sedimentary quartz-rich matrix
22°
o
at
aju e
an ran
Gu ter
Zihuatanejo
terrane
100 km
U/Pb146 Ma
Guanajuato
Figure 6. Geologic map of central Mexico, showing main stratigraphic units of Oaxaquia and the Central, Zihuatanejo, and Guanajuato Terranes
(modified from Ortega et al., 1992). Tr—Triassic; Ju—Jurassic; K—Cretaceous.
Zacatecas Formation
The oldest rocks of the Zihuatanejo Terrane in its northernmost exposure are Triassic in age as well (Fig. 6). They make
up the Zacatecas Formation, which crops out in a small tectonic
window at the western margin of Zacatecas City (Fig. 6; Burckhardt and Scalia, 1906; Ranson et al., 1982; Cuevas-Pérez, 1983;
Monod and Calvet, 1991). This formation is made up of quartzrich turbidites (sandstone and shale) that contain blocks of pillow basalts that have MORB geochemical signatures (Fig. 7;
Centeno-García and Silva-Romo, 1997). The Zacatecas Formation contains fossil ammonites and bivalves of Late Triassic (Carnian) age (Burckhardt and Scalia, 1906; Bartolini et al., 2002).
Its contact with the La Borda Formation of Late Jurassic(?)–Cretaceous age is inferred to have been originally an unconformity,
but it was sheared and detached during Late Cretaceous thrusting and folding (Fig. 3). Rocks of the Zacatecas Formation show
structures associated with two distinct deformational events, one
of them prior to the deformation that is recorded in the Cretaceous rocks as well. The small size of the outcrop prohibits constraints on the tectonic origin of the Zacatecas Formation, but its
lava flows and siliciclastic turbidites are similar to those from the
Arteaga Accretionary Complex, which is exposed in the southern
part of the Zihuatanejo Terrane.
Arteaga Complex
More exposures of Triassic(?) rocks are found in the southern part of the Zihuatanejo Terrane (Fig. 7). Their largest outcrops
are located in the Arteaga, Placeres del Oro, and Tiquicheo areas
(Arteaga Complex) and near Zihuatanejo City (Las Ollas Complex)
(Fig. 8; Centeno-García et al., 1993a, 1993b; Talavera-Mendoza
et al., 1995; Mendoza and Suastegui, 2000). The Arteaga Complex is made up of quartz-rich turbidites (sandstone and shale),
unconformity
163-155 Ma
Arcelia Terrane
blocks of pillow lavas, chert,
serpentinite and limestone
Arteaga Complex
Norian-Carnian
Mexcala Fm.
poly deformed sedimentary
and volcanic rocks
continent-continent collision
felsic lavas and
volcaniclastics
continental affinity
127-133 Ma
Las Lluvias
Ignimbrite
168-179 Ma
unconformity
Taxco Schist,
Zicapa and
Chapolapa
Limestone
Aptian-Albian
Cuautla and
Morelos Fms.
shale and sandstone
foreland-basin fill
Acatlan Complex
mid-Paleozoic
felsic and
andesitic
lavas and
volcaniclastics
shallow marine in the
east, deep marine in
the west
145-137 Ma
Limestone
Aptian-Albian
TeloloapanTerrane
shallow marine
limestone,volcaniclastic
rocks, few andesitic-basaltic
lava flows
Villa de Ayala Fm.
Aptian Albian
MORB basaltic pillow
lavas, IA lavas and
Angao and San
Lucas Fms.
dikes, chert, deep
volcanic turbidites, chert
marine volcaniclastic
felsic and basic lavas
turbidites
shallowing upward
Early Cretaceous
Neocomian
Comburindio and
Mal Paso Fms.
Huetamo region
Cuale
felsic lavas and
Tumbscatío granitoids
and limestone
age not well
constrained
unconformity
Albian-Cenomanian
subaerial few marine
volcaniclastic rocks,
felsic lavas
Aptian
subaerial to marine
shale, sandstone,
evaporites, limestone,
basaltic-andesitic
lava flows
Coastal region
Zihuatanejo Terrane
EAST
Mixteca Terrane
(western Continent-margin)
Figure 7. Simplified stratigraphic columns for the terranes described in the text that are south of the Transmexican Volcanic Belt, except for the Guanajuato Terrane, and include the
Mixteca Terrane and the Teloloapan, Arcelia, and Zihuatanejo Terranes (Guerrero Composite Terrane). Vertical scale shows the age range (in Ma). MORB—mid-oceanic-ridge basalt;
IA—island arc.
Paleozoic
Ladinian
Early Triassic
Carnian
Norian
Rhaetian
Hettangian
Sinemurian
Pliensbachian
Toarcian
Aalenian
Bathonian
Bajocian
Callovian
Oxfordian
Kimmeridgian
Tithonian
Berriasian
Valanginian
Hauterivian
Barremian
Aptian
Albian
Cenomanian
Turonian
Coniacian
Santonian
Campanian
Maastrichtian
WEST
10
0
Tecoman
20
PA
Jilotlán
40
IC
OC
EA
Coalcoman
Pijuamo
Tepalcatepec
Tecalitlán
CIF
Aquila
km
Colima
Nevado de Colima
103°
N
Infiernillo Dam
Zihuatanejo
er
s Riv
a
Bals
Lázaro Cárdenas
Arteaga
Ar/Ar 152-158 Ma
Tumbiscatío
U/Pb 163+3 Ma
Playa Azul
Aguililla
101°
Balsas
River
Huetamo
Zitácuaro
Arcelia
100°
XOLAPA TERRANE
Iguala
Roads
Chapolapa
Chilpancingo
Zicapa
MIXTECO TERRANE
Teloloapan
Taxco
State limit
Rivers
inferred terrane boundary
(strike-slip fault)
inferred terrane boundary
(thrust fault)
Observed terrane boundary
(thrust fault)
Cenozoic volcanic and
sedimentary rocks
Upper Cretaceous to Paleogene
granitoids
CutzamalaFormation
Santonian-Maastrichtian red beds
(overlaps Zihuatanejo and Arcelia
terranes)
Miahuatepec Formation
Upper Cretaceous clastic rocks
foreland basin-fill (overlaps
Arcelia and Teloloapan terranes)
Mexcala Formation
Turonian-Maastrichtian clastic rocks
foreland basin-fill (overlaps
Mixteco and Teloloapan terranes)
Overlapping assemblages
Tejupilco 19°
Jurassic to Cretaceous
migmatites, gneisses, and plutons
Xolapa Terrane
Paleozoic Acatlán Complex
Z I H U ATA N E J O T E R R A N E
Nueva
Italia
102°
Cretaceous MORB pillow lavas,
fine-grained volcanic turbidites
and chert (deep marine)
Cretaceous IAB pillow lavas,
fine-grained volcanic turbidites
and chert (deep marine)
Arcelia Terrane
Lower Cretaceous continental
arc assemblages, marine and
terrestrial rhyolite to andesite lava
flows and epiclastic rocks,
quartz-rich clastic rocks
Aptian-Albian Calcareous
Platform
Mixteca Terrane
18°
Figure 8. Geologic map of southwestern Mexico, showing the simplified geology of the Mixteca, Teloloapan, Arcelia, and Zihuatanejo Terranes (after Campa and Ramirez, 1979;
Ortega et al., 1992; Talavera-Mendoza et al., 1995; Corona-Chávez and Israde-Alcántara, 1999; Mendoza and Suastegui, 2000; Centeno-García et al., 2003). IAB—island-arc basalt;
MORB—mid-oceanic-ridge basalt.
N
Manzanillo
Minatitlán
Zapotitlán
104°
Arteaga Subduction Complex
(Triassic)
Coastal Cretaceous arc assemblage
shallow marine and terrestrial rhyolite,
andesite and some basalt, limestone,
volcaniclastic and basement-derived
clastic rocks
Middle to Upper Jurassic
plutons
Las Ollas Subduction Complex
(age unknown)
Lower Cretaceous arc assemblages
shallow marine andesitic to basaltic
lava flows and volcaniclastic rocks,
massive and reefal limestone (east)
deep marine lava flows, calcareous
debris flows and volcanic turbidites (west)
e
Teloloapan Terrane
deep marin
Huetamo area, Cretaceous
arc assemblage, mostly marine
volcaniclastic rocks, limestone and
some pryroclastic and lava flows
TERRANE
ARCELIA
RRANE
TELOLOAPAN TE
Zihuatanejo Terrane
marine
shallow
296
black and green chert, and mafic tuff that form a matrix that contains blocks and slabs of pillow basalts, diabase, banded gabbros,
chert, and limestone, all deformed in a block-in-matrix structural
style (Centeno-García et al., 2003). Chert layers contain radiolarians of Triassic (Ladinian–Carnian) age (Campa et al., 1982).
Pillow basalts and gabbros have oceanic geochemical signatures
(MORB; Centeno-García et al., 1993a; Centeno-García et al.,
2003). Sedimentary structures preserved in some exposures of
unmetamorphosed turbidites, along with the affinity of the few
fossils found in the sedimentary rocks of the matrix, suggest that
the sequence was deposited in a deep-ocean environment. Apparently the quartz-rich turbidites were contemporaneous with oceanic magmatic activity, as they are interbedded with volcaniclastic rocks (Centeno-García et al., 2003). The block-in-matrix style
of deformation of the Arteaga Complex, as well as its lithological
associations, indicate that it was formed in a subduction accretionary prism. Metamorphism ranges from none to amphibolite
facies; blueschist facies has not been found in the area.
Las Ollas Complex
The Las Ollas Complex forms part of the Zihuatanejo
Terrane and is exposed near Zihuatanejo City (Figs. 7 and 8;
Talavera-Mendoza, 2000). This complex is a tectonic mélange
formed by highly sheared blocks of metabasalt, banded and massive gabbro, metadolerite, ultramafic rocks, and shale and quartzrich sandstone (Talavera-Mendoza, 2000). These blocks are
enveloped in a highly sheared clastic (quartz-rich sandstone) or
serpentinitic matrix (Talavera-Mendoza, 2000). Blueschist facies
were reported by Talavera-Mendoza (1993, 2000). Geochemical
compositions of the basalts are typical of MORB and primitive
oceanic-arc magmas (Talavera-Mendoza, 2000). 40Ar/39Ar and
K/Ar ages obtained from amphibole from several metagabbro
blocks range from 223 Ma to 96 Ma (Permian to early Cenomanian) (Delgado, 1982; A. Iriondo, 2003, personal commun.).
This has been interpreted to be the subduction complex of the
Cretaceous arc (Vidal-Serratos, 1991; Talavera-Mendoza, 1993);
however, its contact relationships with Cretaceous arc-related
rocks, and similarities with the Arteaga Complex, suggest an earlier origin.
Quartz-rich turbidites from the La Ballena Formation of
Oaxaquia (continental Mexico), the matrix of the Taray Formation of the Central Terrane, and the Arteaga and Las Ollas Complexes and the Zacatecas Formation of the Zihuatanejo Terrane
(Guerrero Composite Terrane) have similar and distinctive compositions and detrital-zircon age populations (Centeno-García
et al., 2005; Talavera-Mendoza et al., 2007). Therefore, Triassic
sedimentation of the central and western terranes of Mexico is
linked by provenance. The youngest zircon age populations from
all the samples (latest Permian) are much older than the depositional ages of the turbidites (Carnian–Norian), which means
that there was no active volcanism at that time. In other words,
there is no evidence of Late Triassic continental arc volcanism in
Mexico. Zircon age populations of the Potosi Fan are different
from those of Triassic quartz-rich sandstone from the Caborca
and Cortes Terranes (González-León et al., 2005) but are similar to those from Triassic fluvial sedimentary rocks of Arizona
(Anderson, 2006). This suggests that at the end of the Triassic
the terranes of central and western Mexico may have been to the
north of their present locations.
Based on this evidence, we propose that the margin of the
western paleo-continent of Mexico was passive or rifting at the
end of the Triassic. This passive margin received abundant clastic
sedimentation, forming the large Potosi Fan. Sediments of this
fan were deposited on oceanic crust (Arteaga Basin in Fig. 3).
When subduction started, slivers of the ocean floor were tectonically mixed with the already existing passive-margin quartz-rich
turbidites that were forming the Taray and Zacatecas Formations
as well as the Arteaga and Las Ollas Complexes. Whether the
ocean basin that was covered by sediments of the Potosi Fan was
an active marginal oceanic basin, a marginal backarc basin, or an
open ocean–continent flank is still uncertain. The only potential
evidence of association of the Potosi Fan sediments with tholeiitic oceanic volcanism is the volcaniclastic rocks interbedded
with the siliciclastic turbidites in the Arteaga Complex, as the
volcaniclastic rocks have geochemical signatures between primitive island arc and MORB (Centeno-García et al., 2003).
At least two phases of deformation are found in all the Triassic rocks of Oaxaquia and the Central and Zihuatanejo Terranes.
The first event comprised strong shearing and tight folding, and
the block-in-matrix structures. A second event was recorded
only in the Arteaga Complex. This event deformed the Jurassic
granitoids as well, and it is characterized by a mylonitic fabric.
The third event was common to all the Triassic units and is also
recorded in the Jurassic and Cretaceous cover sediments, and it
is characterized by axial cleavage, open to tight folding, reverse
faulting, and thrusting.
The time of accretion of the Central Terrane with Oaxaquia
is assumed to have been prior to the Middle Jurassic, because the
La Ballena Formation of Oaxaquia and the Taray Formation of
the Central Terrane were deformed and locally metamorphosed
prior to deposition of Upper Jurassic terrestrial volcanic and clastic formations (Tristán-González and Torres-Hernández, 1994;
Jones et al., 1995; Silva-Romo et al., 2000). The Zihuatanejo
Terrane (Guerrero Composite Terrane) was also accreted at that
time, because the Arteaga Complex is cut by granitoids of Middle
Jurassic age as well (Centeno-García et al., 2003).
The subduction zone that formed the Taray and Zacatecas
Formations, and the Arteaga and Las Ollas Complexes, was
probably constructed along the continental margin of Oaxaquia
in Early Jurassic time. Whether the subducting slab was dipping
to the east or to the west has not been determined.
Stage IV: Jurassic Continental Arc of Western Mexico
Erosion and exhumation of the accreted continental slope
sediments and the accretionary complexes occurred prior to the
initiation of Middle to Late Jurassic magmatism. This is indicated
by the major angular unconformity that separates the Jurassic arc
succession from the deformed Triassic rocks of Oaxaquia and
the Central and Zihuatanejo Terranes. Jurassic arc magmatism
has also been identified in the Mixteca Terrane. The Jurassic arc
rocks have different names at different locations; they are hereby
described by their occurrence in different terranes:
Nazas, Huizachal, and La Joya Formations in Oaxaquia
The La Ballena Formation (Oaxaquia) is unconformably
overlain by the volcanic rocks and red beds of the Nazas Formation in the Peñón Blanco, Charcas, and Real de Catorce areas
(Figs. 5 and 6; Silva-Romo, 1993; Tristán-González and TorresHernández, 1994; Barboza-Gudiño et al., 2004). The Nazas Formation is made up of dacitic and minor rhyolitic and andesitic
lava flows and pyroclastic flows, dikes, and porphyritic shallow
intrusives. The volcanic rocks are interbedded with conglomerate, sandstone, and scarce paleosols. Conglomerate is formed
mostly by volcanic clasts and a few clasts of sandstone and shale
derived from the underlying La Ballena Formation. The volcaniclastic conglomerate and sandstone form lens-shaped bedding
with low-angle cross-bedding, interbedded with some debris
flows, suggesting that they were deposited in a terrestrial (fluvial
and alluvial fan) environment.
Although their age has not been well constrained at all
the exposures, there is a report of U/Pb ages as old as 189 Ma
at a subaerial volcanic-sedimentary succession in Huizachal
(Huizachal Formation; Fastovsky et al., 2005), which might not
belong to the same volcanic arc event (Figs. 5 and 6). Rocks of
the Nazas Formation at Real de Catorce yielded U/Pb ages of
172 ± 5 Ma (Barboza-Gudiño et al., 2004). The Nazas Formation changes transitionally upward to shallow-marine volcaniclastic rocks, some evaporites, and thin-bedded limestone, which in
turn become a thick limestone succession in the Peñón Blanco
and Charcas areas (Fig. 6). The basal part of this limestone succession contains late Oxfordian–Kimmeridgian fossil faunas
(Centeno-García and Silva-Romo, 1997). In contrast, there is
an internal angular unconformity in the Real de Catorce locality (Fig. 6), which separates in two units, the terrestrial volcanic
and sedimentary successions (Nazas and La Joya Formations;
Barboza-Gudiño et al., 2004). The upper La Joya Formation
changes transitionally upward to shallow-marine volcanic sandstone and shale interbedded with thin limestone strata. The oldest
fossils reported from the base of the limestone succession in Real
de Catorce are Oxfordian in age (Barboza-Gudiño et al., 2004).
Caopas, Rodeo, and Nazas Formations of the Central Terrane
The volcanic cover of the Taray Formation (Central Terrane;
Figs. 5 and 6) belongs to the Caopas, Rodeo, and Nazas Formations (Córdoba-Méndez, 1964; López-Infanzón, 1986; Jones et
al., 1995). The Rodeo and Nazas Formations are lateral equivalents of the same rocks but named differently in separate outcrops (Díaz-Salgado, 2004). Both units are made up of rhyolitic
to andesitic lava flows and dikes, and pyroclastic deposits that are
interbedded with fluvial sedimentary rocks, mostly sandstone and
conglomerate (Anderson et al., 1990, 1991; Jones et al., 1995;
297
Díaz-Salgado, 2004). The Caopas Formation was formed by
shallow porphyritic intrusives. Felsic volcanic rocks of the Rodeo
Formation yielded a K-Ar age of 183 Ma (López-Infanzón, 1986),
and the Caopas Formation a U/Pb age of 158 Ma (Jones et al.,
1995). Terrestrial volcaniclastic rocks of the Rodeo Formation
are interpreted to have been deformed previous to the deposition
of late Oxfordian limestone (Anderson et al., 1991; Bartolini et
al., 2002). However, in another locality nearby the Nazas Formation changes transitionally upward to shallow-marine calcareous
rocks that range in age from Late Jurassic to Late Cretaceous
(Córdoba-Méndez, 1964; Díaz-Salgado, 2004).
All these volcanic-sedimentary units are interpreted in this
work as the first overlapping succession that stitches the Central
Terrane with Oaxaquia. The Caopas and Rodeo Formations, as
well as the Nazas Formation, are interpreted as continental intraarc assemblages (Jones et al., 1995).
Las Lluvias Ignimbrite of the Mixteca Terrane
Jurassic arc volcanism was also recorded in the Mixteca
Terrane in which ignimbrites, interbedded with fluvial and
shallow-marine siliciclastic deposits, yielded U/Pb ages of 168.2
± 1.2 Ma, 177.3 ± 1.5 Ma, and 179.1 ± 1.5 Ma (Campa and Iriondo, 2003).
Cuale Assemblage and Tumbiscatio Granitoids of the
Zihuatanejo Terrane
Evidence of coeval Jurassic magmatism has been found
in two localities in the Zihuatanejo Terrane (Guerrero Composite Terrane). One of the exposures is NE of Puerto Vallarta
City, in the Cuale mining district, and the other locality is in the
Tumbiscatio region, both along the Pacific Coast (Figs. 7 and
8). Rocks at Cuale contain volcanogenic massive sulfide (VMS)
deposits and are composed of submarine rhyolitic lavas and tuffs,
volcanic sandstone with evolved-arc geochemical affinity (Bissig et al., 2003), and shale that yielded U/Pb ages of 162.4 and
155.9 Ma (Bissig et al., 2003). These rocks are strongly deformed
and partially metamorphosed, and their contact with Cretaceous
unmetamorphosed marine volcanic and sedimentary successions
has not been determined.
Two Jurassic granitoids crop out in the Tumbiscatio region.
They were emplaced in previously deformed sedimentary rocks
of the Arteaga Complex, and vary in composition from granodiorite to granite to quartz monzonite. Their geochemical compositions are typical of calc-alkaline subduction-related granites, which are more evolved than granitoids of Cretaceous and
Cenozoic ages from the same area. Both granitoids show intense
shearing and internal deformation. Grajales and López (1984)
obtained one K/Ar date of Late Jurassic age (158 Ma). U/Pb
isotopic analysis yielded a 163 Ma age, and Ar/Ar ages are 158
and 152.4 Ma (Centeno-García et al., 2003). The igneous rocks
of the Cuale and Tumbiscatio regions have strong similarities
in geochemical composition and age with volcanic rocks of the
Central Terrane (Caopas, Rodeo, and Nazas); thus we suggest
that they probably originated in the same volcanic arc. Therefore,
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the Arteaga Complex was probably accreted to the continental
margin, either near or along the strike from central Mexico.
The Jurassic volcanic event did not produce a thick stratigraphic column and apparently did not have large volumes of
volcanic products. The column changes transitionally upward to
shallow-marine calcareous rocks. Therefore, the lithologic associations and vertical facies changes of this volcanic-sedimentary
event are similar to those of a continental rift. However, the scarce
geochemical analyses from its volcanic rocks suggest an arc setting (Jones et al., 1995). These rocks have been interpreted as the
southern continuation of the Jurassic continental arc that developed along the southwestern margin of North America (Jones et
al., 1995).
It has been proposed that major strike-slip faults were probably active during the arc activity (Mojave-Sonora Megashear;
Jones et al., 1995). This could explain the fact that the Potosi Fan
is south of its possible continental fluvial correlative in Arizona,
as well as the southward displacement of the Tahue Terrane.
Whether or not the Jurassic volcanic event was coeval with
a major transform fault has not been well documented. The
evidence in favor of an important synsedimentary deformation
involving major extension is as follows: (1) Minor synsedimentary normal faults and local angular unconformities are present
within the Jurassic arc volcanic and sedimentary successions,
and pre-Cretaceous mylonitic shearing is recorded in the Jurassic granitoids of the Tumbiscatio region (Zihuatanejo Terrane). (2) Arc magmatism suddenly ceased in the Central Terrane and Oaxaquia, followed by a rapid transgression recorded
in a few meters of transitional sedimentation. (3) Subsidence
rates apparently were significant during the early stages of the
Oxfordian–Kimmeridgian marine sedimentation, because the
calcareous rocks show evidence of deeper sedimentation at
higher stratigraphic levels as well as overall rapid sedimentation. (4) Although fault planes have been obliterated by younger
deformational events, they have been inferred by the rapid lateral changes in thickness and facies of the calcareous succession
through the interval from the end of the Jurassic to the Early
Cretaceous. (5) In addition, major regional lineaments have
been identified in central and eastern Oaxaquia, including the
San Marcos and La Babia Faults (Fig. 1) (Goldhammer, 1999;
Chávez-Cabello et al., 2005).
Stage V: Rifting of the Guerrero Terranes and Formation
of a Complex Arc System
In this section we list the main stratigraphic features of the
volcanic-sedimentary successions of the Guerrero Composite
Terrane and the Mixteca Terrane. Arc volcanism was absent in
Oaxaquia and the Central Terrane through the end of the Jurassic and the Cretaceous. During this period, oceanic crust was
emplaced toward the east of Oaxaquia in the Gulf of Mexico,
and continuous subsidence prevailed throughout the Early Cretaceous, resulting in a thick calcareous platform that covered all the
Central Terrane and Oaxaquia.
Although much detailed work needs to be done in order to
reconstruct the paleogeography of western Mexico during the Cretaceous, the available evidence indicates three important features:
1. Magmatism prograded generally east to west through
time, from the oldest ages in the Oaxaquia and Mixteca
Terranes to the youngest ages in the coastal Zihuatanejo
Terrane. There is some overlap of age ranges for the volcanism among the different terranes, e.g., volcanism of
the Mixteca Terrane overlaps in age with part of the volcanism of the Teloloapan Terrane (Guerrero Composite
Terrane). However, on a large scale, Albian–Cenomanian
volcanism is absent in the Mixteca and the Teloloapan
Terranes, and it is widespread in the coastal region of the
Zihuatanejo and Arcelia Terranes.
2. Magma chemistry changed through time toward a more
primitive melt. The Middle Jurassic volcanic and intrusive rocks in all the terranes show mostly felsic-evolved
continental-arc geochemical signatures, including the
Mixteca Terrane and Oaxaquia. In contrast the Cretaceous
volcanic rocks of the Guerrero Composite Terrane range
from tholeiitic basalts to andesites, with few rhyolites.
They show more primitive island-arc (IA) geochemical
signatures overall, and some even have MORB to oceanicisland basalt (OIB) signatures. The Mixteca Terrane is the
exception to this trend; its magmatism remained evolved,
with continental arc signatures, into the Cretaceous.
3. Within different assemblages of the Guerrero Composite
Terrane there are major differences in the stratigraphy,
sediment composition, and depositional environments.
And the Guerrero Composite Terrane overall is different
from the volcanic-sedimentary rocks of the Mixteca Terrane to the east. In their present distribution, areas with
shallow-marine and terrestrial volcanic-sedimentary successions alternate with areas with deep-marine volcanicsedimentary successions, and suggest a complex paleogeography for that time.
These three features are hereby interpreted as evidence of
intra-arc rifting-translation. We propose, as a hypothesis to be
tested, that the subduction zone might have migrated to the west.
This would have produced thinning of the crust, which in turn
would have originated more primitive IA geochemical signatures
of the magmas and promoted the development of deep basins.
Whether the amount of extension was large enough to develop
oceanic basins and several parallel subduction zones has not
been determined.
The stratigraphy, depositional environments, age, and geochemical affinities of the main units are summarized by terrane.
First, those of southern Mexico are described, following a section
from east to west. Next, Cretaceous rocks of the northern terranes
are described from east to west as well.
Mixteca Terrane
Three localities with Early Cretaceous volcanism have been
identified in the western Mixteca Terrane near the contact with
the Guerrero Composite Terrane: the Taxco Schist and the Chapolapa and Zicapa Formations (Fries, 1960; de Cserna and Fries,
1981; Talavera-Mendoza, 1993; Campa and Iriondo, 2003; Fitz
et al., 2002). The Taxco Schist is made up of submarine andesitic
to rhyolitic lava flows and tuffs interbedded with epiclastic rocks
and quartz-rich sandstone and shale (de Cserna and Fries, 1981;
Talavera-Mendoza, 1993). Its volcanic rocks have a continentalarc geochemical affinity, more evolved than contemporaneous
magmatism from the Guerrero Composite Terrane (TalaveraMendoza; 1993; Centeno-García et al., 1993a). The Zicapa Formation is made up of dacitic to rhyolitic lava flows interbedded
with fluvial deposits (Fitz et al., 2002). The Chapolapa Formation
is composed mostly of marine lava flows and epiclastic rocks.
The abundance of quartzites within the volcanic-sedimentary
successions of the Taxco Schist and Zicapa Formation suggests
that a crystalline basement was exposed during the arc activity.
U/Pb dating of lavas from the Taxco Schist by sensitive
high-resolution ion microprobe (SHRIMP) methods yielded
130–131 Ma ages (Campa and Iriondo, 2004), and from the
volcanic-volcaniclastic rocks of the Zicapa Formation, 127 Ma
(Fitz et al., 2002). Lava flows from the Chapolapa Formation
have 129–133 Ma SHRIMP U/Pb ages. The Taxco Schist shows
one phase of deformation and metamorphism prior to the deposition of Aptian–Albian carbonates. Thus, Early Cretaceous volcanic rocks of the Mixteca Terrane are unconformably covered
by a carbonate platform that ranges in age from Early to middle
Cretaceous (Fries, 1960).
The limestone succession in the western Mixteca Terrane
changes upward to a thick clastic succession (Mexcala Formation) of Turonian to Maastrichtian age (Guerrero-Suastegui,
2004). The Mexcala Formation is made up of alternating sandstone, shale, and conglomerate, deposited in deltaic and submarine-fan environments (Figs. 7 and 8). It is a synorogenic deposit
(foreland basin-fill) associated with regional thrusting and folding of both the Guerrero Composite and Mixteca Terranes at the
end of the Cretaceous. Therefore, the Mexcala Formation is the
first overlapping assemblage that stitches the Guerrero Composite
Terrane and the Mixteca Terrane, and marks the final amalgamation of the Guerrero Composite Terrane to continental Mexico.
Teloloapan Terrane
The Teloloapan Terrane (Figs. 1 and 8) is exposed in the easternmost parts of the Guerrero Composite Terrane. This terrane is
characterized structurally by a complex east-vergent thrust-fault
system. Its rocks are severely deformed and metamorphosed to
low-grade greenschist facies. The Teloloapan Terrane overrides
either Cretaceous platform carbonates or Upper Cretaceous siliciclastic rocks that belong to the Mixteca Terrane (Figs. 7 and 8;
Talavera-Mendoza et al., 1995).
The nature of the basement of the Teloloapan Terrane
remains unknown. Metamorphic rocks of the Tejupilco area
(Fig. 8) were interpreted as a possible basement for the Teloloapan Terrane by Elías-Herrera and Sánchez-Zavala (1990),
and Sanchez-Zavala (1993). These authors suggested that the
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Tejupilco volcanic-sedimentary sequence might represent an arc
assemblage older than the rest of the Guerrero Terrane magmatism. They based this conclusion on U-Pb dates from associated sulfide deposits. The ages they obtained vary broadly from
Carnian (227 Ma) to Oxfordian (156 Ma). However, the same
volcanic-sedimentary rocks were considered a part of the Cretaceous arc assemblage by other authors (Campa and Ramirez,
1979; Talavera-Mendoza et al., 1995).
The arc assemblage of the Teloloapan Terrane consists of
two distinct regions with different volcanic and sedimentary
rocks. The eastern region is characterized by shallow-marine
deposits, and the western region is composed of deeper facies
(Guerrero-Suastegui et al., 1991; Ramírez-Espinoza et al., 1991;
Talavera-Mendoza et al., 1995; Mendoza and Suastegui, 2000;
Guerrero-Suastegui, 2004).The stratigraphy of the eastern region,
from base to top, is made up of basaltic to andesitic pillow and
massive lava flows, volcanic breccias, and pyroclastic flow deposits (Villa de Ayala Formation; Talavera-Mendoza et al., 1995).
These deposits are interbedded with epiclastic sandstone and
conglomerate. Primary structures in the volcaniclastic rocks suggest a marine depositional environment (Guerrero-Suastegui et
al., 1991; Guerrero-Suastegui, 2004). Storm deposits, coral fragments, and other fossils suggest shallow and warm waters. This
unit contains fossil gastropods and bivalves that range in age from
Hauterivian to Aptian (Guerrero-Suastegui et al., 1991; RamírezEspinoza et al., 1991; Talavera-Mendoza et al., 1995).
Geochemical analyses of volcanic rocks of the Villa de Ayala
Formation of the Teloloapan Terrane indicate that the magmatism is calc-alkaline and similar to that of active intraoceanic arcs
(Talavera-Mendoza, 1993; Talavera-Mendoza et al., 1995; Lapierre et al., 1992; Mendoza and Suastegui, 2000; Centeno-García
et al., 1993a). The base of the Villa de Ayala Formation is not
exposed. The maximum thickness is considered to be ~3000 m
(Guerrero-Suastegui, 2004). The volcanic succession of this formation changes transitionally upward to thick, massive reefal
limestone of the Teloloapan Formation. At the base the Teloloapan Formation is composed of intertidal limestone interbedded
with volcaniclastic rocks containing rudists and nerineas of late
Aptian–early Albian age (Guerrero-Suastegui et al., 1991, 1993;
Guerrero-Suastegui, 2004). Thus magmatism ceased prior to the
late Aptian (Guerrero-Suastegui et al., 1991; Mendoza and Suastegui, 2000; Guerrero-Suastegui, 2004). The Teloloapan Formation grades upward into the Pachivia Formation of Turonian age,
which is made up of shale and fine-grained sandstone and shale.
The Pachivia Formation is the western equivalent of the Mexcala
Formation of the Mixteca Terrane and indicates that the Teloloapan and Mixteca Terranes were already in close proximity
(Guerrero-Suastegui et al., 1991; Talavera-Mendoza et al., 1995;
Guerrero-Suastegui, 2004).
The stratigraphy of the western part of the Teloloapan Terrane comprises submarine basaltic, andesitic, and felsic lava
flows and volcaniclastic rocks (Villa de Ayala Formation) deposited in deeper water conditions than the sediments of the eastern
Teloloapan Terrane. It is in transitional contact upsection with
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the Acapetlahuaya Formation, composed of thin-bedded volcanic shale and sandstone at the base, at some localities interbedded with dark, thinly laminated limestone. It changes transitionally upward to shale, with little or no volcanic material at the
top (Campa and Ramirez, 1979; Guerrero-Suastegui, 2004). This
unit has been highly tectonized, making it difficult to calculate
its original thickness and contact relationships. Apparently, the
Acapetlahuaya Formation changes laterally toward the west and
overlies transitionally the volcaniclastic deposits of the Villa de
Ayala Formation. Its upper contact with the Amatepec Formation is highly tectonized. The Acapetlahuaya Formation contains
ammonoids, and radiolarians that are late Aptian in age (Campa
et al., 1974; Guerrero-Suastegui et al., 1993; Talavera-Mendoza
et al., 1995; Guerrero-Suastegui, 2004).
The Amatepec Formation is made up of thin-bedded black
detrital limestone and is devoid of volcanic material. It is interpreted as deep-basin–slope deposits. This formation is tightly
folded and overlies either the Villa de Ayala or the Acapetlahuaya
Formation. It is late Albian to early Cenomanian in age, based on
calcispherulids, planktonic foraminifers, and radiolarians (Campa
and Ramirez, 1979; Guerrero-Suastegui et al., 1991, 1993;
Talavera-Mendoza, 1993; Talavera-Mendoza et al., 1995). The
deep-marine limestone is overlain by turbiditic sandstone-shale
successions of the Miahuatepec Formation (Talavera-Mendoza et
al., 1995). Fossils have not been found, but it is at least post–early
Cenomanian because of its stratigraphic position. The Miahuatepec Formation was deposited, during the amalgamation of the
Zihuatanejo, Arcelia, and Teloloapan Terranes, in a thrust-related
basin (Guerrero-Suastegui et al., 1991; Ramírez-Espinoza et al.,
1991; Talavera-Mendoza et al., 1995; Mendoza and Suastegui,
2000; Guerrero-Suastegui, 2004).
The ages of magmatism of the Teloloapan Terrane have
been poorly constrained by the limited fossils found in the volcaniclastic levels. A few U/Pb isotopic ages from felsic lavas at
the base of the succession range in age from 137.4 to 145.9 Ma
(Tithonian–Hauterivian; Mortensen et al., 2003). Thus, magmatism of the Teloloapan Terrane is in part contemporaneous with
that of the Mixteca, Guanajuato, and Zihuatanejo Terranes.
There are three distinctive differences in the Cretaceous stratigraphy between the Mixteca and Teloloapan Terranes: (1) Volcanism of the Mixteca Terrane is more evolved, and its isotopic
signatures show influence of old continental crust in the magma
generation. In contrast, volcanism of the Teloloapan Terrane is
more primitive and has no traces of contamination by old continental crust (Centeno-García et al., 1993a; Talavera-Mendoza
et al., 1995; Mendoza and Suastegui, 2000). (2) Metamorphic
and quartz clasts are abundant (up to 70%) in the sandstones that
are interbedded with volcanic rocks in the Mixteca Terrane but
are absent throughout the stratigraphic column of the Teloloapan
Terrane. (3) Magmatism ceased in the Mixteca Terrane before
the Aptian, and part of the volcanic-sedimentary succession was
deformed and metamorphosed (Taxco Schist). In contrast, volcanism continued in the Teloloapan Terrane until Aptian–Albian
time, and no internal deformation has been identified.
The arc volcanism of the Mixteca and Teloloapan Terranes
has been interpreted as part of a single arc-backarc system in
which volcanism of the Mixteca Terrane would be the backarc
basin (Cabral-Cano et al., 2000; Monod et al., 1994). An alternative interpretation is that these two terranes belong to different arcs, separated by a double-dipping subduction of an oceanic
basin (Guerrero-Suastegui, 2004).
Arcelia Terrane
Thrust over the Teloloapan Terrane is the Arcelia Terrane
(Guerrero Composite Terrane), which shows deeper marine
facies and less evolved magmatism than the rest of the arc successions of the Guerrero Composite Terrane (Talavera-Mendoza
et al., 1995; Mendoza and Suastegui, 2000). This terrane is made
up of basaltic pillow lavas and ultramafic bodies, black shale and
chert, and fine-grained volcanic turbidites (Fig. 7), all intensively
deformed and partly metamorphosed (Ramírez-Espinoza et al.,
1991; Talavera-Mendoza et al., 1995). The chert layers contain
radiolarians reported as Albian–Cenomanian in age (Dávila and
Guerrero, 1990; Ramírez-Espinoza et al., 1991). Ar/Ar and K/Ar
ages (93.4–105 Ma; Delgado et al., 1990; Ortiz and Lapierre,
1991; Elías-Herrera, 1993) are compatible with biochronology,
but detrital zircon ages from volcanic turbidites are older (mean
age, 130 Ma; Talavera-Mendoza et al., 2007). Geochemical signatures of the Arcelia magmas are similar to those in recent primitive IAs and oceanic basins (MORB) (Talavera-Mendoza, 1993;
Talavera-Mendoza et al., 1995; Mendoza and Suastegui, 2000).
There are no exposures of older rocks in the Arcelia Terrane, and
no clasts of older metamorphic or sedimentary rocks have been
found in its sedimentary strata. Mendoza and Suastegui (2000)
suggest that this terrane is entirely oceanic, that it may have originated as an independent oceanic arc and backarc basin, and that
it represents partly developed oceanic crust. An alternative interpretation is that the Arcelia Terrane could also be a backarc basin
of the Zihuatanejo Terrane (Centeno-García et al., 2003a).
Southern Part of the Zihuatanejo Terrane
Uppermost Jurassic–Cretaceous volcanic-sedimentary assemblages of the Zihuatanejo Terrane can be grouped in three main
regions: northern Zihuatanejo Terrane (Zacatecas area), Huetamo
area, and coastal Zihuatanejo-Colima region (Figs. 7 and 8). The
uppermost Jurassic to Cretaceous strata of the southern Zihuatanejo
Terrane are not as strongly deformed as those in other terranes, and
original contact relationships and complete stratigraphic columns
are well preserved. The strata are characterized by numerous lateral facies changes and internal erosional and angular unconformities. The geographic distribution of the facies is highly irregular,
and it has not yet been determined in detail. Therefore, compiling,
correlating, and synthesizing the stratigraphy of the area is difficult
because it varies considerably from one locality to another. The
stratigraphy of the northern Zihuatanejo Terrane (Zacatecas area)
is described later.
The stratigraphic column of the southern Zihuatanejo Terrane in the Huetamo area is made up of Triassic basement rocks
of the Arteaga Complex, overlain by uppermost Jurassic to Cretaceous volcanic and sedimentary cover. These rocks are thrust
over the Arcelia Terrane (Figs. 7 and 8). Arc-related rocks of the
Huetamo region (Figs. 7 and 8) overall have been formed by a
thick succession of alternating shale, sandstone, and conglomerate, with scattered basaltic pillow lavas, submarine ignimbrite
flows, and other intermediate pyroclastic and epiclastic flows in
the lower parts of the succession (Angao and San Lucas Formations; Pantoja, 1959; Guerrero-Suastegui, 1997). These arcrelated rocks lie unconformably on the Arteaga Complex (Figs. 7
and 8). Fossils of Late Jurassic age have been reported from the
Angao Formation (Pantoja, 1959), although the major exposures
of volcaniclastic rhythmic sedimentary rocks are Berriasian to
upper Aptian (Guerrero-Suastegui, 1997). Their depositional
environment changes upsection from deep to shallow marine.
The volcaniclastic rocks of the San Lucas Formation change
toward the top to thick limestone zones with fossil ammonites,
orbitolinids, and rudists of late Aptian–early Albian age (El
Cajon and Mal Paso Formations; Guerrero-Suastegui, 1997;
Pantoja-Alor and Caballero, 2003). This sequence alternates with
or changes laterally into marine and terrestrial volcanic sandstone
and conglomerate (Comburindio Formation; Guerrero-Suastegui,
1997; Pantoja-Alor and Caballero, 2003). The conglomerate is
covered by massive, thick packets of limestone (Huetamo Formation) that contain fossils of late Albian–Cenomanian age. This
unit is found only in the central parts of the Huetamo region (Pantoja, 1990).
The arc succession of the Zihuatanejo Terrane in the Huetamo
area was deformed prior to the deposition of a thick, subaerial
red-bed succession that is interbedded with volcanic rocks (Cutzamala Formation of Campa and Ramirez, 1979) and is related
to a continental arc of Santonian–Maastrichtian age (AltamiraAreyán, 2002; Benammi et al., 2005).
The oldest Cretaceous rocks of the Zihuatanejo Terrane in
the Zihuatanejo-Colima region of coastal Mexico that have been
penetrated by drilling are Berriasian–Hauterivian in age (Alberca
Formation; Cuevas, 1981). The lower member of the Alberca
Formation is made up of interbedded black shale, sandstone, and
limestone, and some tuff. The upper member is composed mostly
of andesitic-basaltic lava flows interbedded with limestone and
shale. The Alberca Formation changes transitionally upward to
andesitic and basaltic lava flows, with some rhyolitic flows, interbedded with pyroclastic (intermediate tuffs and ignimbrites) and
epiclastic deposits. It contains limestone packets interbedded with
subaerial conglomerate and sandstone, red siltstone, and some
evaporites, and continues into limestone with scarce basaltic pillow lavas at the top (Tecalitlán, Tepalcatepec, and Madrid Formations). The age range of these units, based on their fossil content,
is Barremian to Cenomanian (Grajales and López, 1984).
Along the west coast between the cities of Colima and
Zihuatanejo are exposures of an important succession of red
beds, alternating with lesser amounts of limestone in comparison with other areas of the Guerrero Composite Terrane. The
assemblage is made up of rhyolitic lavas (lava flows, breccias,
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and ignimbrites) and minor andesitic and dacitic lavas (Tecalitlán
Formation, Titzupa-La Unión assemblage, Playitas Formation,
etc.; Ferrusquía et al., 1978; Grajales and López, 1984; Pantoja
and Estrada, 1986; Centeno-García et al., 2003). These units are
interbedded with epiclastic deposits such as tuff, volcanic shale,
and sandstone, and some conglomerate. The assemblage also
contains thin beds of limestone containing orbitolinids, gastropods, and some pelecypods of late Albian–Cenomanian age (Ferrusquía et al., 1978; Grajales and López, 1984). Raindrop marks,
desiccation polygons, and dinosaur footprints can be found in this
succession (Ferrusquía et al., 1978). The lower parts of the Cretaceous succession are missing in the Arteaga region, where nonmarine and shallow-marine volcanic and volcaniclastic rocks of
Aptian–Albian age rest unconformably on the Arteaga Complex.
Overall, Cretaceous volcanic rocks of the southern Zihuatanejo Terrane show geochemical and isotopic signatures that
suggest a transitional composition between oceanic island arcs
and active continental margins (Centeno-García, 1994; Freydier
et al., 1997; Mendoza and Suastegui, 2000). The high potassium
content, abundance of felsic lavas, and trace element abundances
of these volcanic rocks are similar to those observed in IAs where
the crust is thick (>~20 km), allowing magmatic differentiation
(Centeno-García, 1994).
Rocks of the southern Zihuatanejo Terrane are distinctive
from the rest of the terranes because they were deposited in
shallow-marine and fluvial environments, contain fossil vertebrates, and show calc-alkaline volcanism more evolved than that
of the Teloloapan and Arcelia Terranes. Sedimentary rocks interbedded with the volcanic flows contain clasts of their basement
rocks, made up of sandstone, quartz, and mylonitic granite. Thus
its stratigraphy is similar to that of arcs constructed on intermediate crust with a previous history of accretions. The presence of
fossil vertebrates suggests proximity to the continent.
Northern Guerrero Terrane
Following a section from east to west in the northern part of
the Guerrero Terrane, the main stratigraphic characteristic is an
absence of rocks similar to those of the Mixteca or Teloloapan Terrane. Instead, deep-marine volcanic-sedimentary successions of
the Guanajuato Terrane were thrust directly over limestone of the
calcareous platform of Oaxaquia. Contact relationships between
the Guanajuato Terrane and the northern Zihuatanejo Terrane are
unconstrained because the contact is covered by younger units. It
is inferred that the Guanajuato Terrane is overthrust by the Zihuatanejo Terrane on the basis of regional vergence of the structures.
Contact relationships between the Tahue and Zihuatanejo Terranes are unknown because the contact is covered by overlapping
Cenozoic assemblages.
Guanajuato Terrane
The succession at the Guanajuato Terrane has been described
as a complete stratigraphic column of an accreted volcanic arc,
as its assemblages vary from the roots of the arc (gabbros and
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diabases, and dike swarms) to pillow basalts, interbedded with
thin-bedded siltstone, shale, chert, and fine-grained volcanic
sandstone (Figs. 6 and 7; Ortiz-Hernandez et al., 1991; OrtizHernandez, 1992). However, all the different stratigraphic levels
are in the form of tectonic slivers (Fig. 7), with the deepest mafic
levels (gabbro, tonalite, serpentinite, wehrlite, dike swarms)
thrust over the upper stratigraphic levels (pillow basalt and volcanic turbidites).
The uppermost thrust sheet is made up of ultramafic-mafic
rocks of the Cerro Pelón tonalite and the Tuna Mansa diorite.
These ultramafic rocks are thrust over a succession incorporating a diabasic feeder dike swarm, basaltic pillow lavas (La Luz
basalts), rhyolitic tuffs (Cubilete Tuff), and a deep-marine volcaniclastic succession made up of sandstone and shale turbidites, chert, and black detrital limestone (Esperanza Formation;
Quintero-Legorreta, 1992; Ortiz-Hernandez et al., 1992; OrtizHernandez et al., 2003). Basalts of this assemblage show geochemical signatures similar to present primitive volcanic island
arcs (Ortiz-Hernandez, 1992).
The third and lowermost structural level (Fig. 7) is composed of a thick turbidite succession of volcanic graywackes,
quartzites, micritic limestone, radiolarian chert, black shale,
and rare conglomerate resting on basaltic pillow lavas (Arperos
Formation; Ortiz-Hernandez et al., 1992; Lapierre et al., 1992;
Quintero-Legorreta, 1992; Monod et al., 1990; Martínez-Reyes,
1992; Ortiz-Hernandez et al., 2003). Pillow basalts at the base
of the Arperos Formation are more alkaline than the La Luz
basalts and show OI geochemical signatures (Ortiz-Hernandez
et al., 2003). The Arperos Formation is unconformably overlain
by the Aptian–Albian La Perlita Limestone (Ortiz-Hernandez et
al., 2003).
It is difficult to reconstruct the role of the Guanajuato Terrane in the tectonic evolution of western Mexico because of the
lack of enough geochronological data. The only U/Pb zircon
age reported from the area comes from the El Gordo volcanogenic massive sulfide ore deposit (Hall and Mortensen, 2003),
which is considered part of the lowermost succession by Hall
and Mortensen, (2003), but it is at the stratigraphic level of the
second thrust sheet (Cubilete tuff?) in the stratigraphy proposed
by Ortiz-Hernandez et al. (1992). The age of a rhyolite from El
Gordo volcanogenic massive sulfide ore deposit reported by Hall
and Mortensen (2003) yielded a 146.1 Ma U/Pb age. There are
also reports of badly preserved radiolarians from the Arperos Formation that are not in good enough condition to be age indicators
(possibly Valanginian–Turonian in age), but a report of nannofossils suggests a Tithonian–Hauterivian age (Ortiz-Hernandez
et al., 2003). Other ages reported from the Guanajuato area are
from K/Ar analyses and seem to have been reset by later thermal
events (Ortiz-Hernandez et al., 1992, 2003). The sedimentary
rocks of the La Luz and Arperos Formations seem to be distal
volcanic turbidite deposits, but the abundance of limestone associated with the pillow lavas suggests that deposition occurred
above the carbonate compensation depth (Ortiz-Hernandez et al.,
2003). Aptian–Albian limestone of the La Perlita Formation rests
unconformably on the Arperos Formation and suggests that sedimentation and at least one phase of deformation occurred prior
to the Aptian–Albian (Ortiz-Hernandez et al., 2003). Whether or
not this deformation is related to the accretion of the Guanajuato
Terrane to the continental margin has not been determined. At
present the Guanajuato Terrane is thrust over the calcareous
platform of Oaxaquia in the San Miguel de Allende area (OrtizHernández et al., 2002).
Rocks of the Guanajuato Terrane have been correlated with
the Arcelia Terrane, and both were interpreted as having formed
part of an oceanic arc independent of the Zihuatanejo and other
arc terranes (Ortiz-Hernandez et al., 1992). Also, these rocks
are considered relicts of an oceanic basin consumed by subduction related to the arc of the Zihuatanejo Terrane (Lapierre et al.,
1992; Tardy et al., 1994). An alternative preliminary interpretation, based on provenance and stratigraphy, is that the Guanajuato
Terrane may have been the backarc basin of the Zihuatanejo Terrane (Centeno-García et al., 2003).
Zihuatanejo Terrane
The Upper Jurassic–Cretaceous stratigraphy of the Zacatecas area in the northern Zihuatanejo Terrane is very different than
the stratigraphy of the neighboring Central Terrane and Oaxaquia (Figs. 5–7). Whereas the strata in the northern Zihuatanejo
Terrane are mostly composed of volcanic and volcaniclastic
rocks, northern Oaxaquia and the Central Terrane were covered
by a thick, shallow-marine calcareous platform during the Late
Jurassic–Cretaceous (Centeno-García and Silva-Romo, 1997).
This suggests that the Zihuatanejo Terrane was probably undergoing dislocation from the continental margin during that time.
The arc stratigraphy of the Zacatecas area is formed by the
La Borda, Chilitos, and El Saucito Formations (de Cserna, 1976;
Yta et al., 1990; Olvera-Carranza et al., 2001; Olvera-Carranza,
2002). These three formations are made up of pillow basalts and
volcanic breccias, interbedded with thin-bedded siltstone, shale,
chert, and volcanic sandstone and conglomerate, with scarce felsic tuff beds and detrital limestone (Centeno-García and SilvaRomo, 1997; Olvera-Carranza, 2002). The chert layers contain
radiolarian fossils of Neocomian(?) to Aptian–Albian(?) age (Yta
et al., 1990; Olvera-Carranza, 2002). However, older U/Pb ages
have been reported (150–148 Ma) from the base of the succession (Danielson, 2000; Mortensen et al., 2003). Lapierre et al.
(1992) and Freydier et al. (1995) characterized this magmatism
as primitive IA and OI basalts. Sedimentary structures and fossil content suggest that the La Borda, El Saucito, and Chilitos
Formations were deposited as distal turbidites and grain flows in
a volcaniclastic submarine apron (Centeno-García et al., 2003).
These Jurassic–Cretaceous arc successions contain important
volcanogenic, massive sulfide ore deposits (Yta et al., 1990; Danielson, 2000; Mortensen et al., 2003).
Tahue Terane
Cretaceous successions of the Tahue Terrane are exposed
mostly in the Sinaloa de Leyva–Porohui region (Fig. 4). They
were formed by submarine pillow lavas, volcaniclastic rocks,
shale, and limestone. They contain Albian ammonites (OrtegaGutiérrez et al., 1979; Freydier et al., 1995; Gastil et al., 1999),
but Ar/Ar ages from the lavas are younger (86 Ma; Gastil et al.,
1999), suggesting resetting. The basaltic lavas show MORB and
OIB geochemical affinities, but the volcaniclastic rocks are more
evolved and show IA geochemical signatures (Freydier et al.,
1995; Gastil et al., 1999). Although this volcanic succession has
been interpreted as the northern continuation of the Arperos Formation of the Guanajuato Terrane, and part of a major oceanic
basin that originally lay between the Guerrero arc and the continent (Tardy et al., 1994; Lapierre, et. al., 1992; Dickinson and
Lawton, 2001), the stratigraphy does not support such a tectonic
scenario because (1) the Cretaceous volcanic rocks rest unconformably on a Paleozoic basement, (2) the stratigraphy and facies
associations are not indicative of deep-pelagic sedimentation and
oceanic-ridge volcanism, and (3) the Guanajuato successions
apparently are older than the arc assemblages of the Tahue and
other parts of the Guerrero Composite Terrane.
SUMMARY
• The stratigraphy of the Guerrero Composite Terrane of
western Mexico is characterized by a series of terranes
whose basements were formed by Paleozoic to Triassic
fragments of oceanic arcs, continental slope sediments,
and ocean floor assemblages that were accreted to the continent and consecutively rifted and translated.
• Metamorphosed Ordovician volcanic and marine sedimentary rocks and a thick succession of deep-marine turbidites
of the NW Guerrero Composite Terrane (Tahue Terrane)
make up the record of a middle Paleozoic collision and
development of a Carboniferous to Permian passive margin. These rocks might be equivalent to the early Paleozoic
Antler Arc and eugeoclinal sedimentation in the SW Cordillera of North America.
• The continental margin during the early Mesozoic was
located in the middle of Mexico, approximately along the
boundary between Oaxaquia and the Central–Guerrero
Composite Terranes. This continental margin was active
during the Permian–Carboniferous, when a continental arc
developed in Oaxaquia.
• Permian–Carboniferous arc-related magmatism ceased,
and a passive or rifted margin developed along the western continental margin of Mexico, extending throughout
the Triassic. This development is suggested by the thick
submarine siliciclastic turbidite succession that accumulated on the western paleo-continental shelf–slope region
(Potosi Submarine Fan). The siliciclastic fan turbidites are
mostly continent-derived, quartz-rich sandstone, siltstone,
and shale, containing fossils of Carnian–Norian age.
• The Potosi Fan is interpreted as passive-margin deposits,
as there is no evidence of contemporaneous magmatism
either in the stratigraphy or in the provenance.
303
• The siliciclastic rocks of the Potosi Fan extended to the
west in a marginal oceanic basin (Arteaga Basin) that at
present forms the basement of the Zihuatanejo Terrane of
the Guerrero Composite Terrane.
• The first compressional event that deformed the Triassic
rocks originated tight folding, shearing, and axial cleavage
in the La Ballena Formation, and block-in-matrix texture
in the Taray and Zacatecas Formations and the Arteaga
Complex. This deformation was related to subduction
along the early Mesozoic continental margin. It may have
started sometime between the Late Triassic and Early
Jurassic, accreting the turbidites of the Potosi Submarine
Fan, with slivers of the oceanic crust, to the continent.
• Whether the subducting slab was dipping toward the west
or the east is not well constrained, but the accretionary
prism apparently was very wide. Evidence of contemporaneous oceanic arc magmatism is found in the Vizcaíno
Peninsula, where a volcanic sequence of primitive arc affinity is exposed. It is possible that the rocks in the Vizcaino
Peninsula represent a displaced fragment of an oceanic arc
that accreted to the Arteaga Complex of the Guerrero Composite Terrane, but this model needs more evidence.
• Arc-related volcanic and sedimentary rocks unconformably overlie the deformed Triassic rocks of Oaxaquia and
the Central and Guerrero Composite Terranes. They are
characterized by continental rhyolitic to andesitic lava
flows, interbedded with fluvial and alluvial deposits. The
succession shows minor angular unconformities, probably
related to tilting. These rocks have been interpreted as the
southern continuation of the Jurassic continental arc that
developed along the southwestern margin of the United
States. Magmatism was active from ca. 163 to 155 Ma
(Callovian–Oxfordian), although older volcanic rocks
have been reported for eastern Mexico (189 Ma). The
Jurassic arc shows more evolved geochemical signatures
than the subsequent volcanic events.
• During and after the continental arc activity (Late
Jurassic–Early Cretaceous), large amounts of extension
and lateral translations probably occurred, as suggested by
the changes in the stratigraphy. It has been proposed that
major strike-slip faults were probably active during the
arc activity (Mojave-Sonora Megashear). Arc magmatism
ceased in central Mexico, and considerable subsidence
and extension is evidenced by the fast deepening of the
calcareous platform that developed over the arc rocks.
• Major stratigraphic, geochemical, and isotopic differences
are evident in the different Cretaceous stratigraphic assemblages among the Guerrero terranes. They are, from east to
west: Andesitic-basaltic submarine lava flows and tuff (IA
geochemical signatures), interbedded with limestone and
shallow-marine volcaniclastics (Teloloapan Terrane) that
were thrust over contemporaneous but more evolved arc
successions and the calcareous platform of southern continental Mexico (Mixteca Terrane). Ophiolite successions,
304
with deep-marine volcanic and sedimentary rocks with
MORB, OIB, and IA signatures (Guanajuato and Arcelia
Terranes), are placed between the continent and the more
evolved arc in the north (Zihuatanejo Terrane) and between
the two shallow-marine arcs (Teloloapan and Zihuatanejo
Terranes) in the south.
• These major geological differences suggest that intra-arc
rifting was considerable and originated a series of marginal
arc-backarc systems in western Mexico, with complex
paleogeography. Two possible scenarios can be proposed for
the Cretaceous paleogeography of western Mexico: (1) that
there was one single rifting arc, with westward migration
of the magmatism and development of deep-marine intraarc and backarc basins (Guanajuato and Arcelia Terranes);
and (2) that rifting during the end of the Jurassic was large
enough to allow the formation of multiple marginal island
arcs, separated by oceanic backarc basins.
• The proposed timing of the final amalgamation of the
Guerrero terranes to the margin of older terranes that form
the eastern part of Mexico is Turonian to Maastrichtian,
as suggested by the age span of foreland basins associated
with the deformation of the arc. Overlapping the previously deformed Arcelia and Zihuatanejo Terranes, a new
arc developed along the coast by Santonian time.
ACKNOWLEDGMENTS
This paper is a contribution to PAPIIT projects IN109605–3
and IN116599, funded by the Universidad Nacional Autónoma
de México (UNAM), and to projects UC-MEXUS Exotic versus Fringing Arc Models: Implications for the Growth of Continents, and SEP/2003 C02 42642. Special thanks are due J.
Stock, C. Busby, C. Vita-Finzi, and A.E. Draut for their reviews
and comments, which greatly improved the paper.
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Manuscript Accepted by the Society 24 April 2007
Printed in the USA

The Guerrero Composite Terrane of western Mexico

Transcription

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