1.1. EL ANTIMONIO GROUP

The most complete stratigraphic succession of the mostly marine, Permian-Triassic and Lower Jurassic strata of Sonora is exposed in the Sierra del Álamo and Sierra de Santa Rosa localities in northwestern Sonora (Figure 1). An early description of these rocks was made on the Triassic and Jurassic paleontology of both localities (^{Keller, 1928}). Early stratigraphic work on the Permian rocks of Cerro Monos, in the northern part of the Sierra del Álamo was conducted by ^{Cooper and Arellano 1946, 1953} , who named this ca. 500 m thick siliciclastic and carbonate succession the Monos Formation. ^{White and Guiza 1949} reported the stratigraphy for these Triassic rocks and noted their unconformity with the Monos Formation. A complete report on the paleontology of the Monos Formation was presented in Cooper et al. (¹⁹⁵³). ^{González-León 1980} mapped the 3.4 km thick stratigraphic succession of the Sierra del Álamo and divided it into a lower member and an upper member as belonging to Late Triassic and Early Jurassic age, respectively; both members were assigned to the Antimonio Formation. A partly correlative Lower Jurassic section that was studied in detail in the Sierra de Santa Rosa was assigned to the Sierra de Santa Rosa Formation (^{Hardy, 1981}). Other incomplete sections of these strata are scattered at several localities from central to northwestern Sonora (see ^{González-León et al., 2011}).

Figure 1 Base map of northern Sonora and adjacent areas taken from Google Earth (December, 2016). It shows main roads (black dashed lines), towns (white squares) and location of outcrops (yellow stars) to visit in stops 1 to 3 during this field-trip. Other localities mentioned in the manuscript are indicated. Dashed line labeled as MSM indicate approximate trace of the Mojave-Sonora megashear after ^{Anderson and Silver (2005}). 

Subsequent lithostratigraphic and paleontological studies established that the Antimonio Formation consists of 14 upward-shallowing, unconformity bounded sequences (sequences I through XIV), each grading from fluvial to shallow and deep marine environments upwards (^{González-León, 1997}a) (Figure 2), these studies also concluded that the lower part of the Antimonio Formation ranges from the upper Permian to the Upper Triassic (^{Stanley et al., 1994}; ^{Damborenea and GonzálezLeón, 1997}; ^{Estep et al., 1997}a, ^1997b; ^{Lucas et al., 1997}a, ^1997b). González-León et al. (¹⁹⁹⁶) recognized the Triassic-Jurassic boundary in this formation and Lucas et al. (^1997a) recognized the Permian-Triassic boundary. Further details on the Triassic-Jurassic contact were published by González-León (^1997b), Lucas and Estep (^1999a) and González-León et al. (²⁰⁰⁰).

Figure 2 Composite lithostratigraphic column of the El Antimonio Group in the Sierra del Álamo, type section, northwestern Sonora (modified from ^{González-León, 1997}a). 

^{Lucas and Estep (1999}b) revised the use of the Antimonio Formation of the Sierra del Álamo and subdivided the succession into the Antimonio, Río Asunción and Sierra de Santa Rosa formations that were later grouped into El Antimonio Group (^{González-León et al., 2005}). The Antimonio Formation of Lucas and Estep (^1999b) comprises sequence I through sequence VI encompassing upper Permian to Upper Triassic (Carnian) strata. González-León et al. (²⁰⁰⁵), based on updated fossil identifications, reassigned sequences VII to IX to the Río Asunción Formation and sequences X to XIV to the Sierra de Santa Rosa Formation,. The following summarized description of these formations is taken from González-León et al. (²⁰⁰⁵).

1.1.1. ANTIMONIO FORMATION

Sequences I to VI, which compose the Antimonio Formation, range from 100 to 500 m in thickness and are subdivided into seven units (Figure 2). Sequence I disconformably overlies the Permian Monos Formation and consists of calcareous red siltstone, subordinate limestone, fine-grained sandstone and uncommon thin pebble conglomerate. Brachiopods in this sequence that are also common in the Monos Formation suggest a Guadalupian age (^{Lucas et al., 1997}a). Nevertheless, the Monos Formation might be reassigned to the uppermost Permian according to preliminary results reported by ^{Dobbs et al. (2016}), who dated detrital zircons as young as 258 Ma.

Sequence II consists of a basal fluvial conglomerate that is overlain by shallow-marine calcareous red siltstone and sandstone that grades upward into limestone beds with shell remains. The Permian-Triassic boundary was placed tentatively at the base of this sequence (^{Lucas et al., 1997}a), and ^{Steiner et al. (2005}) suggested an Early Triassic (Dienerian) age based on magnetostratigraphy. Sequence III consists of a fluvial conglomerate that has reworked clasts from the Monos Formation that bear the foraminifera Parafusulina antimoniensis that was reported in that formation by ^{Dunbar (1953}) (^{González-León, 1997}a). It grades upwards into sandstone, siltstone and sandy to muddy limestone with ammonoids and conodonts that indicate an Early Triassic (Spathian) age (^{Lucas et al., 1997b}). Sequence IV, although poorly exposed, grades upwards from a clast-supported fluvial conglomerate into marine red sandstone, siltstone, and limestone with ammonoids of Anisian age (^{Estep et al., 1997}a). Similarly, sequence V grades from clast-supported conglomerate into red sandstone, siltstone and limestone with aulacoceratid cephalopods, ammonoids and ichthyosaur bones, probably of the Ladinian or Carnian stage (^{González-León, 1997a}).

The uppermost sequence VI of the Antimonio Formation consists of shallow marine pebbly sandstone that grades upward into sandstone, siltstone and an upper package of massive to finely laminated red mudstone, bioclastic limestone, and fine-grained sandstone with abundant fossils of Carnian age (^{Keller, 1928}; ^{Burckhardt, 1930}; ^{Callaway and Massare, 1989}; ^{Lucas and GonzálezLeón, 1995}; ^{Estep et al., 1997}b, ^{Lucas et al., 2015}). Lucas et al. (²⁰¹⁵) documented the ammonoid assemblage in this package, recognizing the Carnian Sirenites nanseni, Tropites dilleri and Tropites welleri zones.

1.1.2. RÍO ASUNCIÓN FORMATION

Sequence VII, in the lower part of the Río Asunción Formation, has a basal unit (unit 12, Figure 2) of fluvial pebble conglomerate and sandstone that grades upward to calcareous sandstone and coquinoid limestone with bivalves in the middle part of this sequence. The upper part (unit 13) consists of medium to thick-bedded, fossiliferous biostromal limestone with interbedded mudstone and fine-grained sandstone. The biostromes are constructed by abundant scleractinian corals and chambered sponges disjectoporoids and the hydrozoan Heterastridium together with mollusks (ammonoids, gastropods and bivalves), brachiopods and other invertebrate fossils (^{Stanley et al., 1994}; ^{González-León et al., 1996}; ^{McRoberts, 1997}; ^{Damborenea and González-León, 1997}; ^{Goodwin and Stanley, 1997}; ^{Stanley and González León, 1997}; ^{Goodwin, 1999}). Ammonoids and the spherical Heterastridium conglobatum (^{Stanley et al., 1994}) allow assignment of the sequence to the late Norian.

Sequence VIII is a 17 m thick unit consisting of massive calcareous siltstone with bivalves, crinoids and ammonoids from the Rhaetian Amoenum Zone. The lower limestone beds of the overlying sequence IX consist of bioclastic and sandy limestone beds, 2 to 8 m thick with abundant, diverse and reworked ammonoids, bivalves, colonial corals, nautiloids, crinoids, bones and teeth that probably belong to ichthyosaurs and fishes. The ammonoids Rhacophyllites, Sagenites and the Rhaetian index genus Choristoceras were identified from these beds (^{González-León et al., 2000}). Sequence IX varies in thickness from 27 to 43 m and consists of calcareous siltstone, fine-grained sandstone and dark gray laminated to massive mudstone. The mudstone in the uppermost meters of the sequence contains specimens of Rhabdoceras cf. R. suessi Hauer and Choristoceras cf. C. nobile Mojsisovics that characterize the Rhaetian Crickmayi Zone (^{González-León et al., 2000}).

The stratigraphic contact between sequences IX and X represents the Triassic/Jurassic boundary in the El Antimonio Group (^{González-León, 1997}b; ^{Lucas and Estep, 1999}a; ^{González-León et al., 2000}) but the contact is a disconformity making a hiatus. It also represents the contact between the Norian to Rhaetian Río Asunción Formation and the Lower Jurassic Sierra de Santa Rosa Formation (^{González-León et al., 2000}). The boundary is regarded as a disconformity surface, and the lower Hettangian strata are missing. So, the Triassic-Jurassic boundary section, once thought continuous, is incomplete.

1.1.3. SIERRA DE SANTA ROSA FORMATION IN THE SIERRA DEL ÁLAMO

The Sierra de Santa Rosa Formation consists of sequences X to XIV in the Sierra del Álamo but its upper part is missing because of faulting. The missing upper part crops out in the Sierra de Santa Rosa locality, where sequences were not defined. The lower part of the 60 m thick sequence X is composed of a base-erosive, laterally continuous, coarse-grained to pebbly sandstone that fines upwards into calcareous siltstone, containing the ammonoid Sunrisites sunrisensis Guex (^{GonzálezLeón et al., 1996}). This ammonoid characterizes the uppermost Hettangian Sunrisense Zone (^{Taylor et al., 2001}). The upper part of this sequence is composed of interbedded siltstone, dark gray calcareous mudstone and up to 1 m thick bioclastic limestone beds with ammonoids and bivalves. Coroniceras n. sp. of the middle part of this sequence was assigned by Taylor et al. (²⁰⁰¹) to the lower Sinemurian Trigonatum Zone, while Badouxia mexicana and B. canadensis in these beds have a range that straddles the uppermost Hettangian and lowermost Sinemurian stages (see figure 3 in ^{Taylor et al., 2001}). Bivalves of this sequence, including Weyla (Lywea) unca, were described by ^{Scholz et al. (2008}). The lower part of sequence XI is marked by a 20 m thick, upward-fining, clast-supported pebble conglomerate that grades upward into sandstone and siltstone of fluvial origin. Most of the middle part of the sequence is cut out by a dioritic intrusion, and its upper part consists of massive to finely laminated calcareous mudstone and siltstone with ammonoids from the lower Sinemurian (Involutum and Leslei Zones) (^{Taylor et al., 2001}). Scholz et al. (2008) also reported bivalves including Weyla alata, Weyla (W.) bodenbenderi, W. titan and W. unca. A basal pebble-conglomerate of sequence XII is overlain by sandstone and sandy coquina beds that grade upsection into massive mudstone/ siltstone with thin beds of bioclastic limestone and interbedded ash-fall tuffs beds. The limestone contains Weyla (Lywea) unca and W. (W.) alata and other bivalves as well as ammonoids denoting the Sinemurian Carinatum and Jamesi Zones (Pálfy and ^{González-León, 2000}; ^{Taylor et al., 2001}). Sequence XIII and XIV compose the uppermost 615 m of the Sierra de Santa Rosa Formation in the Sierra del Álamo. Sequence XIII has in its middle part turbidite beds with poorly preserved ammonoids that are late Sinemurian age (^{Pálfy and González-León, 2000}), whereas sequence XIV is mostly terrigenous and barren of fossils.

Figure 3 Geologic map of the Sierra de Santa Rosa (figure to the left) showing the lower, middle and upper members of the Lower Jurassic Sierra de Santa Rosa Formation (modified from ^{Hardy, 1981}) and stratigraphic columns (figure to the right) of measured sections 3, 4 and 5 (reported in ^{Damborenea and González-León (1997}): Location of these sections is indicated in the geologic map. 

1.1.4. SIERRA DE SANTA ROSA FORMATION IN THE SIERRA DE SANTA ROSA

The Lower Jurassic strata in the Sierra de Santa Rosa were first reported by ^{Keller (1928}) and ^{Flores (1929}), followed by ^{Jaworski (1929}) who provided a list of molluscan fossils that he assigned to the Lower Jurassic. ^{Hardy (1981}) described the stratigraphy and named the succession as Sierra de Santa Rosa Formation that he subdivided into lower, middle, and upper members encompassing a thickness of 1460 m (Figure 3A); however, this is an incomplete thickness estimate as the formation is thrust over the Proterozoic basement of the region and its upper part is covered by younger volcanic rocks.

According to the description of ^{Hardy (1981}), the lower member consists of alternating cross-bedded sandstone, calcareous mudstone, lesser volcanic pebble conglomerate and sandy limestone. The middle member is composed of bluish gray limestone, sandy fossiliferous shale, sandstone and tuffaceous mudstone beds. In its upper part it grades into fine-grained sandstone and limestone. The shale and limestone contain the best preserved fossils in the formation. The upper member consists of shale, sandstone, volcanic conglomerate and limestone. ^{Jaworski (1929}) described fossils collected from the middle member, including seven bivalve species, among them Weyla (Weyla) mexicana introduced as a new species and one ammonoid (Arietites sp.), in addition to Deroceras sp., which was previously reported by ^{Flores (1929}). Hardy (1981) considered the lower member to likely be of Triassic age.

^{Damborenea and González-León (1997}) reported stratigraphic details of these members from three measured sections (Figure 3B) and illustrated bivalves. Section 3, which is thrust over older rocks, is located in the southwestern part of the Sierra de Santa Rosa (Figure 3) and includes part of the lower and middle members. The lower member there includes in its lower part upward-fining successions of conglomerate, coarseto fine-grained sandstone, mudstone and siltstone, which origin was interpreted as fluvial. The middle part of this member consists of shallow marine fine-grained sandstone, calcareous shale and bioclastic to sandy limestone, where one limestone bed yielded Weyla (W.) alata von Buch (Damborenea and GonzálezLeón, 1997) and Weyla (W.) bodenbenderi (^{Scholz et al., 2008}) and the ammonoid Paltechioceras from the uppermost Sinemurian (^{Pálfy and González-León, 2000}). The upper part of this lower member is composed of interbedded coarseto fine-grained sandstone, siltstone, calcareous mudstone and bioclastic and encrinitic limestone with occasional solitary corals.

The upper part of section 3 consists of interbedded calcareous mudstone and shaly to sandy, fossiliferous limestone beds of the lower part of the middle member. The middle member in this area, as shown by partial sections 3, 4 and 5, consists of thinto medium-bedded fossiliferous limestone (yielding bivalves and ammonoids including the early Pliensbachian Metaderoceras) and interbedded calcareous, bluish mudstone and subordinate fine-grained sandstone beds. A large number of bivalve taxa from this member were described in ^{Damborenea and González-León (1997}) and by ^{Scholz et al. (2008}), including W. (W.) alata, Weyla (W.) bodenbenderi, Weyla (Lywea) unca and W. titan and two mound-like carbonate buildups in the section are constructed by colonial corals and bivalves (González-León et al., 2005; ^{Hodges et al., 2015}). The partly exposed upper member reported in section 5 consists of calcareous, fineto medium-grained and locally cross bedded sandstone, calcareous mudstone with the ammonoids Metaderoceras sp., Dubariceras sp., and Fuciniceras sp. (^{Pálfy and González-León, 2000}) and sandy bioclastic limestone.

Ammonoids from the lower, middle and upper members reported by Pálfy and ^{González-León (2000}) and subject to more ongoing studies indicate that the Sierra de Santa Rosa Formation, in the mountains of the same name, ranges in age from the late Sinemurian to the early Pliensbachian.

Other partly exposed successions of this formation occur in at least four other localities of northwest Sonora. For instance, in the Pozo de Serna locality, 50 km west of the Sierra de Santa Rosa Mountains (Figures 1 and 4), a 750 m thick section of sandstone, shale and limestone yielded ammonoids that were first assigned to the Upper Jurassic (^{Beauvais and Stump, 1976}). These fossils were later variously reassigned to the lower Pliensbachian (^{Linares et al., 1997}), Sinemurian to Bajocian-Bathonian (^{Calmus et al., 1997}) and uppermost Sinemurian (^{Lucas et al., 1999}). Based on an assemblage dominated by species of Polymorphites this section was reassigned to the lower Pliensbachian by Pálfy and ^{González-León (2000}). The youngest section of this formation crops out in the Sierra La Jojoba, located ~ 40 km northwest of the Sierra de Santa Rosa (Figure 1 and 4) and according to preliminary identification of early dactylioceratid ammonoids it is now assigned to the Pliensbachian rather than the lower Toarcian (Pálfy and González-León, 2000). Weyla (W.) bodenbenderi is present in the Pozos de Serna locality, W. titan is present in the Sierra La Jojoba and Weyla (Weyla) alata is present in both localities (^{Scholz et al., 2008}).

Figure 4 Correlation of the Jurassic sections of Sierra del Álamo, Sierra de Santa Rosa, Pozo de Serna and Sierra La Jojoba (locations shown in Figure 1). It shows the lower, middle and upper members of the section of the Sierra de Santa, stratigraphic position of the bivalve Weyla and ages according to the identified ammonites. 

1.2. EARLY MESOZOIC ARC MAGMATISM

A northwest-southeast trending magmatic arc, that was well developed by early Mesozoic time in southwestern North America, was constructed at a high angle to the trend of the late Paleozoic truncated margin of Laurentia (^{Stone and Stevens, 1988}; ^{Walker, 1988}; ^{Barth et al., 1990}, 1997; ^{Busby-Spera, 1988}; ^{Busby-Spera et al., 1990}; ^{Dickinson and Lawton, 2001}; ^{Riggs et al., 2016}). The early phase of this magmatism started in Permian time and continued into the Triassic as was recorded by plutonic suites of Sonora and southeastern California. The Sonoita suite (^{Riggs et al., 2016}) of Sierra Los Tanques (Figure 1) and surrounding areas of northwestern most Sonora apparently shows a magmatic pulse from ~ 275 to 221 Ma (^{Arvizu et al., 2009}; ^{Riggs et al., 2012}; ^{Arvizu and Iriondo, 2015}), whereas several plutonic suites in the Mojave Desert range in age from ~ 260 to 207 Ma (U-Pb ages in ^{Barth and Wooden, 2006}).

A renewed, Jurassic magmatic pulse that occurred in an extensional arc is recorded by the thick accumulation of juxtaposed volcanic and volcaniclastic facies rocks and interbedded eolian craton-derived quartzarenites that are intruded by penecontemporaneous plutons (^{Busby-Spera et al., 1990}). Among the oldest outcrops known of this arc are those of the lower Colorado River region in southwestern Arizona and southeastern California, where volcanic and plutonic rocks have yielded U-Pb ages ca. 190 - 158 Ma (^{Tosdal and Wooden, 2015}) and the Mount Wrightson Formation of southern Arizona that accumulated between 183 and 170 Ma (in ^{Haxel et al., 2005}). Other successions in southern Arizona have U-Pb ages between ~ 170 and 165 Ma, e.g. the Cobre Ridge Tuff (^{Riggs et al., 1993}) and the Topawa Group (^{Haxel et al., 2005}). Volcanic and sedimentary succession in southeastern Arizona with ages from approximately 200 to 170 Ma (^{Lawton et al., 2012}).

Outcrops of the Jurassic arc in northern Sonora are recognized at several localities. Volcanic and plutonic rocks of northern Sonora, mostly within the southern Papago domain, have ages from ca. 180 to 165 Ma (^{Anderson et al., 2005}), whereas an age of ca. 180 Ma was reported from metarhyolites at Estación Llano (^{Poulsen et al., 2008}) (Figure 1). From west of the town of Cucurpe (Figure 1), ^{Mauel et al. (2011}) reported a complete sedimentary and volcanic succession composed of the Basomari and Rancho San Martín formations. The Basomari Formation is a fluvial unit composed of conglomerate, sandstone and siltstone. The Rancho San Martín Formation consists of eolian quartzarenite, litharenite, dacitic ash flow tuffs, volcaniclastic conglomerate, andesitic flow breccia and lacustrine limestone. Interbedded tuffs in these units yielded U-Pb ages of ca. 190 Ma for the Basomari Formation and of 168.4 ± 1.2 Ma for the Rancho San Martín (U-Pb, zircon) (^{Leggett et al., 2007}; ^{Mauel et al., 2011}; ^{Lawton and Molina-Garza, 2014}), whereas a pluton that cuts the Basomari Formation was dated at ca. 181 Ma (^{Lawton and Molina-Garza, 2014}). The Rancho San Martín Formation is unconformably overlain by the marine, Upper Jurassic Cucurpe Formation. In northeastern Sonora, volcanic and plutonic rocks dated by Anderson et al. (²⁰⁰⁵) yielded ages U-Pb of ca. 174 Ma, whereas detrital zircons in a quartzarenite succession yielded a younger population with peaks at ca. 162 Ma (^{González-León et al., 2009}), and unpublished data from one of us (CG-L) indicate U-Pb zircon ages of granites at ca. 184 and 174 Ma, and a rhyolite succession of 170 Ma.

The ages of rocks of the Jurassic arc in northern Sonora have been settled between ca. 190 and 162 Ma, and their outcrops were considered by ^{Anderson et al. (2005}) to be restricted to the north of their Mojave-Sonora domain. This domain is proposed as a zone of deformation associated with the Mojave-Sonora megashear, a left-lateral fault that transported the Caborca block from latitudes of southern California to its present position between ca. 165 - 150 Ma (^{Anderson et al., 2005}). At the south of this domain lies the Caborca block with rocks of the El Antimonio Group. Nevertheless, the Jurassic volcanic arc and plutonic rocks that crop out on the Caborca block in the south of the megashear, in Sierra Los Tanques and surrounding areas of northwesternmost Sonora (Figure 1) have U-Pb ages from ca. 176 to 160 Ma (^{Quintanar-Ruiz, 2008}; ^{Izaguirre-Pompa, 2009}; ^{Arvizu and Iriondo, 2015}).

1.3. LATE JURASSIC CUCURPE FORMATION

Near the town of Cucurpe, the Cucurpe Formation crops out in the La Cumarosa area, where it unconformably overlies the Rancho San Martín Formation, and at Rancho La Colgada where its base is not exposed (Figures 1 and Figure 5). At the La Cumarosa, the Cucurpe Formation is unconformably overlain by the Lower Cretaceous Morita Formation and at Rancho La Colgada it is overlain by the Lower Cretaceous Rancho La Colgada Formation (^{Mauel et al., 2011}). According to the description of Mauel et al. (²⁰¹¹), the Cucurpe Formation consists of a ca. 1.5 km thick succession of thinly bedded shale, mudstone, tuffaceous siltstone and sandstone, subordinate granule-pebble conglomerate and scarce andesitic flows that represent upward-coarsening marine prodeltaic strata. In the section at La Cumarosa, Mauel et al. (²⁰¹¹) divided the formation into a fine-grained lower member that accumulated in pelagic to hemipelagic environments and an upper member that represents deposits of low-density to high-density turbidity currents and rare debris flows, slumps and slides. At some intervals, ammonoids, bivalves and belemnoids are present.

Figure 5 Stratigraphic column and correlation of the Cucurpe Formation at the La Cumarosa and Rancho La Colgada sections. These localities are near the town Cucurpe in north-central Sonora, as shown in Figure 1 (modified from ^{Mauel et al., 2011}). 

The Rancho La Colgada section was first reported by ^{Rangin (1977}), who considered it as late Oxfordian based on ammonoids. ^{Villaseñor et al. (2005}) later reported that this section is 515 m thick and is composed of massive to finely laminated gray to black shales with interbedded siltstone, fine-grained sandstone and subordinate mafic volcanic flows. Common ammonoids and bivalves of this section indicate an Oxfordian and early Tithonian age, but no Kimmeridgian fossils were identified. A 1 m thick intraformational conglomerate bed near the middle part of the section separates the Oxfordian and Tithonian strata. From the La Cumarosa section, ^{Mauel et al. (2011}) constrained the age of the Cucurpe Formation by U-Pb geochronology from ca. 158 to 149 Ma and also reported Idoceras cf. I. densicostatum of early Kimmeridgian age.

1.4. INTERPRETATION OF TECTONIC SETTING

Different hypotheses are proposed to interpret the tectonic setting of the Permo-Triassic and Jurassic magmatic arcs. Iriondo and ^{Arvizu (2009}) and ^{Riggs et al. (2009}) recognized the Permian magmatism in Sonora to be associated with initiation of subduction along the southwestern margin of Laurentia; younger Permian and Triassic plutons of southeastern California and western Arizona were recognized as subduction-related arc rocks (^{Barth et al., 1997}; Barth and Wooden, 2006). According to the age of this arc (~ 275 - 221 Ma, as noted before), it must have been formed contemporaneously with movement of the California-Coahuila sinistral transform fault (^{Dickinson, 2000}; ^{Dickinson and Lawton, 2001}), that was active from 281 to 248 Ma and that truncated the southwestern margin of Laurentia. The California-Coahuila fault model proposes that the Caborca block was translated southeast, to its present position during Permian-Triassic time instead of during Jurassic time as suggested by the Mojave-Sonora megashear model.

^{Arvizu and Iriondo (2015}) depicted the Permian-Triassic arc as extending from western North America across eastern Mexico and into northwestern South America following the final assembly of Pangea. ^{Riggs et al. (2016}) indicated that the Permian arc started to develop dominantly subaqueously and offshore in southwestern North America as there is no detrital record of it in continental rocks of that age. Riggs et al. (2016) inferred that the offshore arc that later connected with the continent at ca. 230 Ma (late Carnian time) was probably associated with intra-arc deformation that subsequently exposed it to erosion and shed detritus to sedimentary retro-arc units, such as the Chinle Formation.

Sedimentation in the El Antimonio basin was coeval with development of the magmatic arc during latest Permian and Triassic time, as recorded by geochronology data. Ages of detrital zircons from the El Antimonio Group and the laterally equivalent, mostly fluvial Barranca Group (^{González León et al., 2009}) of central Sonora record inception of the arc magmatism at ca. 290 Ma and its waning in the latest Triassic, with peak ages at 255 and 228 Ma (Figure 6A). Also, igneous clasts dated from the Antimonio and Río Asunción formations range in age from ca. 280 to 240 Ma (^{Riggs et al., 2009}, ²⁰¹⁰; ^{Lindner, 2013}). Similarly, new detrital zircon ages from 291 to 258 Ma reported by ^{Dobbs et al. (2016}) from the mixed siliciclastic and carbonate rocks of the Monos Formation indicate that this unit likewise records Permian arc magmatism. The older ages of the zircons grains in the Monos Formation, the El Antimonio and Barranca groups suggest that arc magmatism in the region might have started by the earliest Permian, at ca. 290 Ma.

Figure 6 Histogram and relative probability curves for the less than 300 Ma detrital zircons dated from A) samples of El Antimonio and Barranca groups (data from ^{González-León et al., 2009}), and B) from samples of the Jurassic Sierra de Santa Rosa, Basomari and Lily formations (data from González-León et al., 2009) and from the Cucurpe Formation (data from ^{Mauel et al., 2011}). 

The tectonic setting of the El Antimonio basin has been proposed to be a fore-arc basin (^{Stanley and González-León, 1995}; González-León, 1997a; ^{Lucas et al., 1999}; González-León et al., 2005). The Lower Jurassic (Hettangian-Sinemurian-Toarcian) Sierra de Santa Rosa Formation records deeper-water depositional environments and increased rates of sedimentation regarding to the Antimonio and Río Asunción formations (^{González-León et al., 2005}). The deepening of the basin was coincident with initiation of Jurassic arc magmatism at ca. 200 Ma, as suggested by published ages of detrital zircon grains from this (González-León et al., 2005) and other Jurassic formations of northern Sonora (Figure 6B) (^{González-León et al., 2009}; ^{Mauel et al., 2011}).

Nevertheless, interpretations of the original position of this basin are speculative. Strata of the Monos Formation and El Antimonio Group altogether have been interpreted either as an allochthonous terrane that accreted to the Caborca block based mostly on its fossil content, or as strata that were relocated during the Jurassic by the Mojave-Sonora megashear, along with the Caborca block from southern California to its present-day position (^{Stanley and González-León, 1995}; González-León, 1997a; Marzolf and ^{Anderson, 2005}).

However, a different interpretation for these rocks is that they were deposited close to the arc and near the present-day location, on the Caborca block, which had been previously displaced from southern California by the California-Coahuila transform fault (^{Riggs et al., 2016}). A petrographic study carried out by ^{Lindner (2013}) on fluvial sandstone of the Antimonio and Río Asunción sequences (coupled with the ages of clasts and detrital zircons) suggests that their compositionally and texturally immature detritus should have been derived from and recorded the unroofing of the nearby Permo-Triassic arc that was located to the north of the basin. Similarly, Riggs et al. (²⁰¹²) established a geochemical link between detrital zircon grains in the El Antimonio and Barranca groups with Triassic plutonic suites of the Mojave Desert.

^{Dickinson and Lawton (2001}) recognized a distinction between the Permo-Triassic and Jurassic arcs, suggesting a hiatus of arc magmatism during Middle Triassic time. According to these authors, the older arc was formed to the breakup of Pangea and the younger arc developed during intracontinental extension at early phases of the breakup of Pangea. The Jurassic magmatism was of high-K, calc-alkaline composition and was emplaced episodically from ca. 190 Ma to near 160 Ma in southern Arizona and northern Sonora (^{Tosdal and Wooden, 2015}). It is considered as a continental extensional arc that in northeastern Sonora was constructed across the Proterozoic and Paleozoic basement and in northwestern most Sonora the plutons intruded the Permo-Triassic arc rocks. In north-central Sonora, the region known as the southern Papago domain lacks exposures of an older basement (^{Anderson et al., 2005}). The Middle Jurassic arc magmatism ended when the NWSE, fault-bounded basins in the region of Sonora and Arizona formed contemporaneously with the opening of the Gulf of Mexico. Opening of the basins may be related to opening of the Gulf of Mexico, or they may be related either to rollback of the subducting slab (^{Lawton and McMillan, 1999}; ^{Dickinson and Lawton, 2001}) associated with the Jurassic arc, or to strike-slip faulting related to the Mojave-Sonora megashear (^{Anderson et al., 2005}; ^{Busby et al., 2005}).

A sparse and younger magmatism that is mostly present in the Papago domain falls in the age range from 160 to 145 Ma and consists of alkaline volcanic and plutonic rocks and interbedded sedimentary strata (^{Tosdal et al., 1989}). ^{Anderson et al. (2005}) considered this magmatism unrelated to the calc-alkaline Jurassic arc magmatism and instead they relate it to trans-tensional mechanisms associated with the megashear. Alternatively, ^{Mauel et al. 2011} considered it related to early extension of the Cucurpe-Altar rift, in which the Cucurpe Formation was deposited and identified as the likely source of zircon grains of 149 Ma that are present in the younger part of this formation (Figure 6B). The Cucurpe Formation is important as it records onset of extension and marine incursion of the Gulf of Mexico waters into central Sonora (Mauel et al., 2011). Coeval strata in northeastern Sonora and southeastern Arizona are continental strata and interbedded volcanic rocks of the Glance Conglomerate that compose the lower part of the Upper Jurassic and Lower Cretaceous Bisbee Group. ^{Dickinson et al. (1986}) and Dickinson et al. (¹⁹⁸⁹) proposed that the Bisbee Group accumulated in the Bisbee basin, which was formed by rifting associated with the incursion of an aulacogen related to opening of the Gulf of Mexico. During the Late Jurassic, the northwest-trending Cucurpe-Altar and Bisbee basins were parallel depocenters separated by the basement highs of the Aldama platform in Chihuahua (^{Haenggi, 2002}) and its probable continuation, the Cananea high in northern Sonora (^{McKee and Anderson, 1998}). Well documented outcrops of the Cucurpe Formation in Sonora are only known from near the town of Cucurpe, in the Arroyo La Cumarosa and Rancho La Colgada sections (Figures 1 and 5). The La Cumarosa section is ca. 1.5 km thick and its U-Pb age ranges from ca. 158 to 149 Ma (late Oxfordian to early Tithonian), whereas the Rancho La Colgada column is an incomplete thin section with abundant ammonoids and bivalve fauna that constrain its age to the late Oxfordian and early Tithonian (^{Villaseñor et al., 2005}). The Rancho La Colgada column, however, lacks the ammonoid faunas indicating the latest Oxfordian, the Kimmeridgian and the earliest Tithonian. An intraformational conglomerate, 1 m thick near the middle part of this section that has clasts of dark shale, volcanic rocks and abundant reworked ammonites, belemnites and bivalves may be a condensed section that spans the Kimmeridgian. Similarly, the single Kimmeridgian ammonite found in the Rancho La Cumarosa section was recovered from a conglomerate composed of volcanic and limestone clasts with reworked belemnites of the middle part of the section and that is closely associated with strata recording soft-sediment deformation. Mauel et al. (²⁰¹¹) correlated both intervals as of possible Kimmeridgian age (Figure 5).