Abstract Epithermal deposits form in tectonically active arc settings and magmatic belts at shallow crustal levels as the products of focused hydrothermal fluid flow above, or lateral to, magmatic thermal and fluid sources. At a belt scale, their morphology, geometry, style of mineralization, and controls by major structural features are sensitive to variations in subduction dynamics and convergence angle in arc and postsubduction settings. These conditions dictate the local kinematics of associated faults, influence the style of associated volcanic activity, and may evolve temporally during the lifetime of hydrothermal systems. Extensional arc settings are frequently associated with arc-parallel low- to intermediate-sulfidation fault-fill and extensional vein systems, whereas a diversity of deposit types including intermediate-sulfidation, high-sulfidation, and porphyry deposits occur in contractional and transtensional arc settings. Extensional rift and postsubduction settings are frequently associated with rift-parallel low-sulfidation vein deposits and intermediate- and high-sulfidation systems, respectively. At a district scale, epithermal vein systems are typically associated with hydrothermal centers along regional fault networks, often coexistent with late fault-controlled felsic or intermediate-composition volcanic flow domes and dikes. Some districts form elliptical areas of parallel or branching extensional and fault-hosted veins that are not obviously associated with regional faults, although veins may parallel regional fault orientations. In regional strike-slip fault settings, dilational jogs and stepovers and fault terminations often control locations of epithermal vein districts, but individual deposits or ore zones are usually localized by normal and normal-oblique fault sets and extensional veins that are kinematically linked to the regional faults. Faults with greatest lateral extent and displacement magnitude within a district often contain the largest relative precious metal endowments, but displacement even on the most continuous ore-hosting faults in large epithermal vein districts seldom exceeds more than several hundred meters and is minimal in some districts that are dominated by extensional veins. Veins in epithermal districts typically form late in the displacement history of the host faults, when the faults have achieved maximum connectivity and structural permeability. While varying by district, common unidirectional vein-filling sequences in low- and intermediate-sulfidation veins comprise sulfide-bearing colloform-crustiform vein-fill, cockade, and layered breccia-fill stages, often with decreasing sulfide-sulfosalt ± selenide abundance, and finally late carbonate-fill; voluminous early pre-ore barren quartz ± sulfide fill is present in some districts. These textural phases record cycles associated with transient episodes of fluid flow triggered by fault rupture. The textural and structural features preserved in epithermal systems allow for a field-based evaluation of the kinematic evolution of the veins and controlling fault systems. This can be achieved by utilizing observations of (1) fault kinematic indicators, such as oblique cataclastic foliations and Riedel shear fractures, where they are preserved in silicified fault rock on vein margins, (2) lateral and vertical variations in structural style of veins based on their extensional, fault-dominated, or transitional character, (3) extensional vein sets with preferred orientations that form in the damage zones peripheral to, between, or at tips of fault-hosted veins, and (4) the influence of fault orientation and host-rock rheology and permeability on vein geometry and character. Collectively, these factors allow the prediction of structural settings with high fracture permeability and dilatancy, aiding in exploration targeting. Favorable structural settings for the development of ore shoots occur at geometric irregularities, orientation changes, and vein bifurcations formed early in the propagation history of the hosting fault networks. These sites include dilational, and locally contractional, steps and bends in strike-slip settings. In extensional settings, relay zones formed through the linkage of lateral fault tips, fault intersections, and dilational jogs associated with rheologically induced fault refraction across lithologic contacts are common ore shoot controls. Upward steepening, dilation, and horsetailing of extensional and oblique-extensional fault-hosted vein systems in near-surface environments are common and reflect decreasing lithostatic load and lower differential stress near surface. In these latter settings, the inflection line and intersections with branching parts of the vein system intersect in the σ 2 paleostress orientation, forming gently plunging linear zones of high structural permeability that coincide with areas of cyclical dilation at optimal boiling levels to enhance gangue and ore precipitation. The rheological character of pre- and syn-ore alteration also influences the structural character, morphology, and position of mineralized zones. Adularia-quartz-illite–dominant alteration, common to higher-temperature upflow zones central to intermediate- and low-sulfidation epithermal vein deposits, behaves as a brittle, competent medium enabling maintenance of fracture permeability. Lateral to and above these upflow zones, lower-temperature argillic alteration assemblages are less permeable and aid formation of fault gouge that further focuses fluid flow in higher-temperature upflow zones. Fault character varies spatially, from entirely breccia and gouge distally through progressively more hydrothermally lithified fault rocks and increasing vein abundance and diminishing fault-rock abundance proximal to ore shoots. In poorly lithified volcaniclastic rocks or phreatic breccia with high primary permeability, fault displacement may dissipate into broader fracture networks, resulting in more dispersed fluid flow that promotes the formation of disseminated deposits with low degrees of structural control. In disseminated styles of epithermal deposits, mineralization is often associated with synvolcanic growth faults or exploits dikes and phreatic breccia bodies, feeding tabular zones of advanced argillic and silicic alteration that form stratabound replacement mineralized zones. In lithocap environments common to high-sulfidation districts, early, laterally continuous, near-surface barren zones of advanced argillic alteration and silicification form near the paleowater table above magmatic-hydrothermal systems. In many high-sulfidation deposits, these serve as aquitards beneath which later hydrothermal fluids may localize mineralization zones within permeable stratigraphic horizons, although deeper mineralization may also be present within or emanating from faults unrelated to lithocap influence. Silicified lithocaps may contain zones with high secondary structural permeability that localize ore through the formation of zones of vuggy residual quartz and/or elevated fracture densities in the rheologically competent silicified base of the lithocap, often along or emanating laterally outward from ore-controlling faults. Syn-ore faults in such settings may form tabular, intensely silicified zones that extend downward below the lithocap.

ABSTRACT Upper Triassic and Lower to Middle Jurassic strata in the Plomosas uplift of central Chihuahua accumulated in backarc and rift settings, respectively. The succession, as much as ~3250 m thick, consists of four stratigraphic units. The Cerro El Carrizalillo Formation (Carnian–Norian), a volcanic-lithic shallow-marine succession deposited in the (newly named) El Carrizalillo backarc basin, is characterized by predominantly Triassic detrital zircon ages. The overlying Plomosas Formation consists of three members: (1) the Cerro de Enmedio Member (Hettangian–Toarcian), a succession of conglomerate, siltstone, and shallow-marine carbonate strata deposited during the onset of extension in Chihuahua; (2) the Cerro Nevado Ignimbrite Member (176 ± 1 Ma; late Toarcian), a widespread ash-flow tuff; and (3) La Sofía Member (Aalenian–Callovian?), consisting of alluvial-fan conglomerate, fluvial sandstone, tidal sandstone and siltstone, and delta-plain red beds characterized by rapid facies changes, lithic compositions, and diverse Proterozoic, Paleozoic, and Triassic detrital zircon ages characteristic of a rift-basin setting. The extensional basin in which the Cerro de Enmedio and La Sofía members accumulated is termed the Plomosas basin. Improved age control provided by U-Pb maximum depositional ages from detrital zircon and U-Pb zircon analyses of the ignimbrite indicates that the Cerro El Carrizalillo Formation is partly correlative with the Chinle Formation of the Colorado Plateau, and the Plomosas Formation is equivalent to eolianites of the Glen Canyon and San Rafael Groups of the Colorado Plateau. Detrital zircon ages and sandstone textures are consistent with both proximal and distal sediment sources along the Laurentia-Gondwana suture and adjoining Grenville basement of Laurentia, including sources in northern Mexico and the composite Appalachian orogen. Although the depositional setting of the Cerro El Carrizalillo Formation was not connected to fluvial systems of the Chinle Formation, subsequent eolian transport of voluminous sediment to the overlying Cerro de Enmedio and La Sofía members from the Colorado Plateau ergs is suggested by the composition and texture of some sandstone, thick siltstone accumulations, and detrital zircon characteristics that broadly resemble those of the Colorado Plateau eolianites. Thick siltstone in the upper part of La Sofía Member is interpreted as deflated fine-grained sediment that was transported downwind from a time-equivalent erg to accumulate in shallow-marine and coastal-plain settings of the Plomosas basin.

Abstract The mine caves of Naica (Chihuahua, Mexico) are famous because they host large gypsum crystals. Mine works intersected new caves hosting the largest crystals in the world in the year 2000. From 2006 these caves became the object of a multidisciplinary research project with the goal of inferring their ages, the boundary conditions for their formation and the mechanisms inducing their development. Several other scientific aspects were also considered, including palynology, mineralogy, microbiology, physiology, hydrogeology and astrobiology. From 2006 to 2009, scientists and explorers tried to ensure the complete documentation of these natural wonders because they were expected to be accessible for only a few years. As a result of their location c. 160 m below the natural groundwater level, they were predicted to be flooded with thermal water as soon as dewatering of the mine ceased. This occurred at the end of 2015, so that the lower part of the mine is already submerged and in the near future the giant crystal caves will also disappear. Theoretically, it is still possible to maintain these incredible wonders for future generations, but this seems highly unlikely. Soon the crystals will be submerged below c. 150 m of hot water, restarting their incredible slow growth.

Tascotal Mesa fault is the principal component of Tascotal Mesa transfer zone within the Rio Grande rift of Texas (USA) and Chihuahua (Mexico). Strata and structures along the zone attest to ~290 m.y. of tectonic and magmatic activity, from at least late Paleozoic time onward. The transfer zone comprises the Tascotal Mesa and newly documented Christmas Mountains–Grapevine Hills faults, as well as the Terlingua Creek pull-apart complex at the right step between those two dextral zones. Strike-slip (to ~1 km) and dip-slip (to ~735 m) displacements have occurred in the zone during the past 30–27 m.y.; young faults of the transfer zone displace mid-Pleistocene caliches. Stable isotope and palynologic data from travertines in the transfer zone indicate ascent of warm waters (25°–35 °C) along faults as recently as mid- to late Pleistocene time. Older, basement-rooted structural anisotropies are present in the Tascotal Mesa transfer zone but not all have been reactivated during Cenozoic rifting. Geophysically constrained physical models integrated with field data demonstrate that the Terlingua Creek pull-apart basin likely formed in cover strata that were detached from basement, as the orientations of surficial and buried basement structures differ markedly. Dip-slip displacement predominates on pull-apart faults, with significant dextral slip. Analysis of the role of the Tascotal Mesa transfer zone in Rio Grande rifting revealed that it and the flanking grabens (Presidio to the northwest; Redford to the southeast) are all parts of the Border Corridor transform zone. This transform zone interconnects rift segments from Mesilla graben to the Sunken Block and includes both transfer zones and grabens. Right-transtensional deformation, as manifested in historic earthquakes, accounts for differing orientations of transform (northwest) versus rift (north) grabens. Petrographic and geochronologic data indicate ascent of lavas of rift geochemical character in both the Tascotal Mesa transfer zone and the Border Corridor transform zone from ca. 30 Ma onward. K-Ar ages were determined for basalt (24.73 ± 1.96 Ma) and trachyte (25.42 ± 0.64 Ma) emplaced within the Tascotal Mesa transfer zone. Magmatism is bimodal; olivine basalt and/or hawaiite predominates. Basalts at the junctions of rift grabens and the Border Corridor transform zone entrain mantle and lower-crustal xenoliths.

Abstract Of all the countries in the world considered to be oil rich, Mexico is the only one that consistently has been losing production and reserves in the last ten years. Even though Mexico has five major producing provinces: two for oil (the Southeast and the Tampico–Misantla basins) and three for gas (the Sabinas, Burgos and Veracruz basins), and has seven more with potential, (California, Gulf of Cortès, Chihuahua, Sierra Madre Oriental, Sierra de Chiapas, Progreso shelf, and the deep Gulf of Mèxico), its output and reserves have declined consistently. Many reasons can be attributed for these results, and as this note proves, least of them is the country’s endowment of oil and gas resources. The problem is that Mexico, since 1938, has had only one oil company responsible for all of its upstream activities and even though Pemex’s performance is comparable with that of most of the majors’ (it is world’s third largest in terms of production), it is impossible that all the remaining potential of the entire country can be found and produced with only one company, no matter how large, wealthy, efficient, technologically advanced, and successful it can be. The good news is that once the country opens up for third-party participation in exploration, which will eventually take place, results are going to be spectacular. So far there has only been a timid opening for development and exploitation opportunities.