bluuebunny/crossref_metadata_2025_split huggingface dataset:
Hueco Mountains Introduction
Authors: Simo J. A. (Toni) , Wahlman Greg P. , Stoklosa Michelle. L. , Beall Jen L. 
Published: April 2015

Abstract
J. A. (Tom) Simo, Greg P. Wahlman, Michelle L. Stoklosa, Jen L. Beall
The Permian was a remarkable geological period, and it is reflected in the abundance of important sedimentary mineral resources. It represents the maximum stage of Pangeacontinental accretion, a gigantic continent from pole to pole surrounded by an all-encompassing ocean. The large Permsylvanian-Lower Permian Gondwana polar ice cap was at its maximum and later was partially replaced by large lakes. Chemically, Permian seas reached the most extreme values of carbon, sulfur, and strontium isotopic ratios, but returned abruptly to normal values close to the end of the Permian period (Scholle et al., 1995). Fauna and flora show an increasing provincialism that culminated at the end of the Permian with one of the largest extinction events in Earth’s history.
The Permian rocks reflect those extreme physical, chemical, and biologic changes. As such, the Permian sedimentary record is unique to explain changes in the biosphere, and the occurrence and distribution of economic deposits. For instance, from early to late Permian, source bed accumulation shifted from a period of major to minor occurrences respectively. The abundance of carbon in the sedimentary record is in part the reason of large early-middle Permian in age reserves of oil and gas (minimum global estimates are 28.4 MMM13 of oil and 6642 TCF of gas; Mazzullo, 1995). Similarly, the global cycle of phosphorous followed that of carbon (phosphorite deposits are early to middle Permian; Herring, 1995). The high carbon
Permian Platforms and Reefs in the Guadalupe and Hueco Mountains The
Capitan Margin of the Guadalupe Mountains
Authors: Harris Paul M. (Mitch) 
Published: April 2015

Abstract
The Late Permian (Guadalupian) mixed carbonate/siliciclastic sequences of the Delaware Basin, one of the long-lived subbasins of the Permian Basin, are well knovvn both for their classic outcrop exposures revealed by basin and range structuring in the Guadalupe Mountains and for their prolific hydrocarbon production (Figure 18). A large number of stratigraphic and sedimentologic studies have established the Capitan reef and associated facies as a model for the understanding of carbonate facies in a shelf margin setting and of reciprocal sedimentation relations between a shelf and basin. Early studies focused on biostratigraphy, lithostratigraphy, and early concepts of reciprocal sedimentation. Focus shifted in the 1970’s and 1980’s to analysis of depositional facies and processes and on the relatively new understanding of early diagenesis of reef margins. More recently, the outcrops have been analyzed from a cyclostratigraphy and sequence stratigraphy perspective. It will be interesting to see the impact of a refined stratigraphic fi-amework on the direction of future facies, paleo-ecological, and diagenetic studies.
Providing the initial interest in the area were the superb field studies and subsequent detailed reporting of the geology of the southern Guadalupe Mountains by King (1942, 1948). The book by Newell et al. (1953) on the Capitan did much to further enhance the outcrops as research models for sedimentary geologists. The critical treatment of the Capitan sedimentology by Dunham in the late 1950’s and 1960’s, culminating in his detailed 1972 guidebook, stimulated interest and added new understanding. Dunham’s work, plus the
Stratigraphic Evolution of Deep-Water Architecture
Authors: Covault J.A. , Crane W.H. , Bernhardt A. , Jobe Z.R. , Armitage D.A. , Fosdick J.C. , Shultz M.R. , Clark J. , Lowe D.R. , Graham S.A. 
Published: April 2015

Abstract
This large format (11 × 17 inch) all color outcrop atlas and field guide was produced for the SEPM Research Conference held in Chile in February, 2009. It contains a wealth of information on the world class deep water outcrops of the Cretaceous of the Magallanes Basin in the Ultima Esperanza District, Chilean Patagonia. This book covers the significant outcrops in the region the Punta Barrosa Formation, CerroToro Fm., and the Tres Pasos Fm.
Outcrops of the Magallanes Basin in the Ultima Esperanza District, Chilean Patagonia
Authors: Graham S.A. , Lowe D.R. 
Published: April 2015

Abstract
The Magallanes Basin SEPM Field Conference, February 2009, showcases outcrops of Cretaceous deep-water clastic strata exposed in the Ultima Esperanza District of southernmost Chile from Puerto Natales northward to Torres del Paine National Park. Why travel to the ‘end of the Earth’ to see these deep-water deposits? We believe that the deep-water succession in the Magallanes Basin of Chilean Patagonia is destined to join a select set of outcrop systems such as the Tanqua Karoo of South Africa (e.g., Wickens and Bouma, 2000; Johnson et al., 2001) and Brushy Canyon Formation of west Texas (e.g., Beaubouef et al., 1999; Gardner et al., 2003) as a world-class outcrop analog for buried, petroliferous deep-water systems. Magallanes Basin outcrops are notable for several key features: (1) Involvement in a latest Cretaceous – early Tertiary fold-thrust belt, providing nearly continuous down-depositional-dip 2-D outcrops for ~100 km, with local 3-D exposures provided by folding and topography; (2) Deep excavation and many bare-rock surfaces created by Late Cenozoic glaciation; (3) Contrasting styles of deep-water systems stratigraphically stacked during basin evolution, from unconfined and/or weakly-confined turbidite systems through highly-confined channelized systems through progradational failure-dominated delta slope with numerous channels and sand-filled mini-basins. The variability of the Magallanes Basin fill over a relatively small area makes the exposures of the Ultima Esperanza District worthy of the attention of the international sedimentologic community.
But it has not always been so. Cretaceous outcrops in the Magallanes Basin of the Ultima Esperanza District
Controls on Deep-Water Stratigraphic Architecture
Authors: Romans B.W. , Fildani A. , Hubbard S.M. 
Published: April 2015

Abstract
The effect of inherited attenuated crust from the closure of the predecessor backarc basin led to a relatively narrow orogenic belt during the Magallanes foreland development and a short distance from arc to foredeep. The attenuated crust heritage also provided continuous basinal subsidence (contributed to by fold-thrust belt loading and ophiolitic block obduction),which permitted long-lived (&gt;20 my) deep-marine deposition and accumulation of &gt;4000 m of turbiditic sediment that filled the basin axially in a north to south direction (Figs. ii.1A and C). Three distinct formations that reflect three distinct phases of deep-water deposition with different stacking patterns are featured in this document: the Punta Barrosa Formation, the Cerro Toro Formation, and the Tres Pasos Formation.
These three formations were deposited with contrasting stratigraphic architectures that we relate to two general factors: (1) variability in amount and type of source material (i.e., changes in provenance and/or staging area) and (2) variations in the basin shape throught time. Changes in the source and staging areas are represented by clear sedimentological differences, including the sandstone-and mudstone-dominated Punta Barrosa Formation with banded slurry beds, the conglomeratic channel-fill deposits of the Cerro Toro Formation, and the sandstone packages and mudstone-rich mass transport deposits of the Tres Pasos Formation slope system (Figs. ii.1B and C; see following page).
Basin morphology controls the general lay-out of depositional systems (e.g., channel dimensions, degree of confinement, dispersal patterns, etc.), which influences the distribution of sediment and resultant stacking patterns. We suggest
Deep-Water Sedimentary Facies of the Magallanes Basin
Authors: Fildani A. , Romans B.W. , Hubbard S.M. 
Published: April 2015

Abstract
The Tres Pasos Formation is a continental margin-scale progradational mudstone- to siltstone-rich slope succession. The lower part of this formation is characterized by an architecturally variable suite of sandstone-rich channel and sheet elements punctuated by mudstone-rich mass transport deposits. Sandstone-rich sedimentary bodies comprise massive sandstone (mostly high-density turbidity current deposits; S1 and S3 sensuLowe, 1982), intrabasinal mudstone-clast conglomerates, and various finer-grained turbidite facies (i.e., Bouma divisions; Bouma, 1962). The sandstone bodies exhibit a highly-variable internal architecture, including complex scour-and-fill features and lateral facies changes. Large-scale mudstone-dominated mass transport deposits (MTDs) typically contain mud-matrix supported debris flow deposits mixed with slide/slump blocks of variable sizes and are common between sandstone packages. The upper part of the Tres Pasos Formation is dominated by turbiditic mudstone and siltstone, hemipelagic mudstone, and sparse scours filled with coarse-grained pebbly material interpreted as by-pass conduits.
Outcrop 2. Punta Barrosa Formation Sheet Complex, Rio Serrano Section (New Roadcut)
Authors: Fildani A. 
Published: April 2015

Abstract
Outcrop accessibility: easy Outcrop Coordinates: 51.2177°S, 72.9606°W Refer to outcrop 2 on location map
A recently excavated roadcut at the Rio Serrano bridge (Fig. 2.1A), located just south of the Rio Serrano, is an easily accessible outcrop of the upper Punta Barrosa Formation. Stratigraphically positioned at the same level as the Marina’s Cliff outcrops (from which it is visible), this outcrop offers good lateral continuity of tabular architecture with few clear examples of scouring and amalgamation. Individual sandstone packets (elements) are almost entirely composed of slurry-beds with some intebedded packets of conventional fine-grained turbidites and mudstone (S4 and S6).
The slurry-beds in the roadcut exposure display a beautiful array of internal banding (micro-, meso-, and macro-banding, sensuLowe and Guy, 2000), consisting of bands of mud-rich (dark) and cleaner (light) sandstone within individual beds. Band thickness varies throughout beds, both laterally and vertically (B). Few beds evolve from meso-banding at the base into micro-banding at top (C). Water escape features are present throughout the beds, commonly as vertically oriented sheets in pale bands (D), sheared sheets in dark bands (D), and throughout massive beds (E; photo slightly higher in measured section). We interpret the slurry-beds to be the result of relatively rapid load fallout from turbidity currents, causing mud entrapment within sand falling out of suspension. The banding is interpreted in a similar way to the process described by Sylvester & Lowe (2004), whereby during rapid sedimentation, the high proportion of mud
Introduction to the Cerro Toro Formation in the Silla Syncline
Authors: Bernhardt A. , Crane W.H. 
Published: April 2015

Abstract
Outcrop accessibility: easy Outcrop Coordinates: 51.1199°S, 72.9701°W Refer to outcrops 4 and 5 on location map
The Silla Syncline is located within the Torres del Paine National Park east of Lago Pehoe and south of Lago Nordenskjöld. The Cerro Toro Formation in the area comprises more than 1100 m of deep-water strata within which Crane (2004) recognized and mapped three major coarse-grained channel complexes. These correspond to the informally named Pehoe, Paine and Nordenskjöld members, from oldest to youngest (Figs. iii.1, iii.2).
The Pehoe channel complex, consists of two conglomerate units, Pehoe A and B, separated by a 100-m-thick sequence of thick-bedded sandstones and thin interbedded mudstone units (see outcrop #4). The Paine member is subdivided into the Paine A, Paine B, Laguna Negra debris flow deposit, and the Paine C (see outcrop #5). Paine C is the largest channel in the section with a width of 2.5 to 3 km and a minimum thickness of 200 m (Figs. iii.1, iii.3 and iii.4). The Nordenskjöld member is exposed as a near continuous, roughly circular outcrop in the axis of the syncline north of the park highway (Fig. iii.3). This member is divided into two major subdivisions, Nordenskjöld A and Nordenskjöld B, separated by a thick debris flow deposit (Figs. iii.1 and iii.4).
The various channel complexes throughout the Silla Syncline section shifted locations as they were emplaced. The
Review of Interpretations for the Paine Channel Complex at Silla Syncline
Authors: Crane W.H. , Hubbard S.M. , Fildani A. , Romans B.W. 
Published: April 2015

Abstract
Multiple models have been proposed to account for the origin of channel and out-of-channel deposits in the Cerro Toro Formation at the Silla Syncline. The complex stratigraphic relationship between coarse-grained channel, and fine-grained out-of-channel deposits has been a topic of considerable debate in the scientific literature. Winn and Dott (1979), Beaubouef et al. (1996), and Beaubouef (2004) propose aggradational channel-levee models for the channel complexes present in the Parque Nacional Torres del Paine (Fig. iv.1A, B). Conversely, Coleman (2000), Crane (2004), and Crane and Lowe (2008) have proposed variations on an evolutionary model that invokes erosional confinement of channel sediments in background Cerro Toro Formation mudstone (Fig. iv.1C, D). The high-energy axial portion of the best-exposed and most well studied channel complex (Paine C of Crane et al., 2008) is a minimum of 4 km wide and the Silla Syncline provides only an oblique cross-section through the complex (Fig. iv.1D). If the system is levee confined, the coeval levees must have added substantially to the cross-sectional width of the channel complex; post-depositional structures both east and west of the syncline limit the preserved width to only slightly more than the channel axis in most areas. As a result it is difficult to discern whether the erosional margins preserved in outcrop represent the edges of an incisional channel complex, or the eroded inner margins of extensive levees.
Outcrop 4. Pehoe Member
Authors: Bernhardt A. , Jobe Z.R. , Lowe D.R. 
Published: April 2015

Abstract
Outcrop accessibility: easy Outcrop Coordinates: 51.1199°S; 72.9701°W Refer to outcrop 4 on location map
The Pehoe channel complex consists of two conglomerate units, Pehoe A and B (nomenclature of Crane, 2004), separated by a 100 m-thick sequence of thick-bedded sandstones and thinly interbedded mudstone units (Fig.4.1A and B). The Pehoe A member consists of the Pehoe A conglomerate and the Pehoe A thick-bedded sandstone and mudstone. The Pehoe B member is subdivided into the Pehoe B conglomerate and the associated Pehoe B mass transport deposits.
Outcrop 5. NW Margin of the Paine ‘C’ Channel Complex, Silla Syncline
Authors: Crane W.H. , Lowe D.R. 
Published: April 2015

Abstract
Outcrop accessibility: easy Outcrop Coordinates: 51.1199°S; 72.9701°W Refer to outcrop 5 on location map
The northwestern portion of the Paine C channel complex (Fig. 5.1A) is easily accessible from the Torres del Paine park highway. Exposures of the Paine C continue throughout the axis of the Silla Syncline from the park highway south to Laguna Negra (Fig. 5.1B). Stratigraphically, the Paine C lies directly above a regionally correlated mass transport complex informally named the Laguna Negra Debris Flow (Fig. 5.1C). The channels within the complex show overall paleoflow toward the southeast and south (Figs. iii.5 and 5.1C). The greatest preserved thickness of channel deposits trends southeast from section 11 to section 21 at the southeastern edge of the syncline (Fig. 5.1B). Given the orientation of the channel complex with respect to paleoflow, the limbs of the Silla Syncline expose a somewhat oblique cross-sectional view of the Paine C channel complex (Fig. 5.1C).
Measured sections along the west limb of the syncline demonstrate that the Paine C thickens progressively to the south by the addition of sediment at the top of the section. A minimum of six stacked channel margins are present between the park highway and Lago Sarmiento Chico (Fig. 5.1C). Channel margins are identified by erosional surfaces which may or may not be mudstone draped and against which sandstones, conglomerates and interbedded sandstone and mudstone units onlap. The approximate locations of
Outcrop 6. Cerro Toro Channel Margins, Sierra del Toro
Authors: Jobe Z.R. , Bernhardt A. , Fosdick J.C. , Lowe D.R. 
Published: April 2015

Abstract
Outcrop accessibility: N face - moderate; S face - extremely difficult Outcrop Coordinates: N face = 51.0781°S, 72.6999°W; S face = 51.1284°S, 72.6813°W Refer to outcrop 6 on location map
Deposits of the Cerro Toro Formation on Sierra del Toro represent the most proximal axial channel belt deposits preserved in the Magallanes Basin outcrop belt, based on regional paleogeographic interpretations (Scott, 1966; Hubbard, 2006; Hubbard et al., 2008b). Scott (1966) provided the first description of conglomeratic deposits on Sierra del Toro; Winn and Dott (1979) interpreted this location as part of an elongate submarine fan that filled the basin axis from north to south.
Cerro Toro Formation outcrops on Sierra del Toro include at least three conglomeratic units, each of which is interpreted to represent a submarine channel complex. These channel complexes were deposited within an axial channel belt (Fig. 6.1A and 6.1B). The units are hereby informally named, from oldest to youngest, the “Condor” (Barton et al., 2008), “Guanaco”, and “Wildcat” channel complexes.
Outcrop 7. Wildcat Channel Complex Axis-to-Margin Architecture, Sierra del Toro
Authors: Jobe Z.R. , Bernhardt A. , Hubbard S.M. , Lowe D.R. 
Published: April 2015

Abstract
Outcrop accessibility: difficult Outcrop Coordinates: 51.0852°S, 72.6541°W Refer to outcrop 7 on location map
The Wildcat channel complex is up to 5–6 km wide and 330 m thick, making it the largest exposed on Sierra del Toro. Hubbard and Shultz (2008) suggest that this channel complex is stratigraphically equivalent to the upper two-thirds of the conglomeratic portion of the Cerro Toro Formation at Cerro Castillo, located due south of Sierra del Toro adjacent to the south shore of Lago del Toro. A portion of the eastern Wildcat channel margin was characterized by Hubbard et al. (2008b) (outcrop featured in Fig. 7.2E, referred to as “Sarmiento Vista” by Hubbard et al., 2008b).
The eastern margin of the Wildcat channel complex is well exposed on the northeast face of the mountain, displaying 200 m of conglomeratic channel fill thinning until its final pinchout (Figs. 7.1B and 7.2). This exposure allows for a direct correlation of beds along a ~3 km transect oblique to depositional strike (1.5 km when projected parallel to strike; Fig. 7.3). The slope of the margin averages approximately 7.5° over this distance, although it is partitioned into a steep ‘wall’ at its base, near the channel complex axis, and a shallower ramp nearer the final pinchout (Fig. 7.3). As a result, the eastern margin is characterized by a “steerhorn” cross-sectional profile. Paleoflow measurements taken at the margin of the channel complex
Outcrop 8. Channel Margins in the Cerro Toro Formation, Cordillera Manuel Señoret
Authors: Hubbard S.M. , Romans B.W. 
Published: April 2015

Abstract
Outcrop accessibility: variable Outcrop Coordinates: 51.4716°S, 72.6508°W Refer to outcrop 8 on location map
Conglomeratic deposits of the Cerro Toro Formation attributed to deposition in a large-scale basin axial channel belt are well exposed in the Cordillera Manuel Señoret, north of Puerto Natales between Cueva del Milodon and Lago Toro. The conglomeratic succession is informally called the “Lago Sofia Member” because of the presence of Laguna Sofia in this area (Scott, 1966). The large injectite complex that is the focus of Chapter 9 is present in the Cordillera Manuel Señoret on the south shore of Lago Sofia (Fig. 8.1A).
The channel belt is characterized by low sinuousity, demonstrated with outcrop mapping and the collection of extensive paleocurrent data (Fig. 8.1A). Outcrop exposures of the channel belt margin are present on the north faces of Cerro Benitez and Cerro Mocho (Fig. 8.1B, C). Because of poor accessibility, the margin at Cerro Mocho cannot be easily visited.
A levee interpretation for fine-grained material adjacent to the channel belt is based on a series of key observations: (i) paleocurrent measurements indicative of flow divergence (50° to 100°) measured from out-of-channel units as compared to those taken from inside the channel belt container; (ii) progressive thinning of sandstone beds away from the channel belt margin; (iii) evidence that the eroded channel margin was poorly indurated, including a stepped profile and injection of channel fill into out-of-channel strata; (iv) deposits that record slumping on the
Outcrop 9. Clastic Injectites in the Cerro Toro Formation, Lago Sofia
Authors: Hubbard S.M. , Romans B.W. , Graham S.A. 
Published: April 2015

Abstract
Outcrop accessibility: easy Outcrop Coordinates: 51.5394°S; 72.6291°W Refer to outcrop 9 on location map
The injectites at Lago Sofia were first reported by Scott (1966) and Winn and Dott (1979). The first comprehensive evaluation of the features was done by Schmitt (1991), with a more recent summary published by Hubbard et al. (2007), who noted the geometrically analogous nature of the injectites to similar features in the North Sea.
The injectites at Lago Sofia are exposed in 3-D, characterized by a near vertical outcrop of channel deposits in the lowest part of the succession. The middle part of the succession where the injectites are most prevalent is exposed on an ancient terrace, allowing for plan-view mapping of the injectite complex. The upper part of the stratigraphic succession is exposed sub-vertically, permitting visualization of the cross-cutting relationships between injectites and host strata (Fig. 9.1).
A series of three channel bodies (C1–C3) are laterally offset and progressively younger eastward. Each channel body is associated with injected bodies at its margins. Both margins of C1 experienced sediment remobilization and injection. Channel C2 experienced injection solely on its western margin; the associated injectite, I3, bifurcates and is observed to cross-cut &gt;125 m of overlying stratigraphy. Channel C3 is the smallest, as is its accompanying injectite (I4).
Outcrop 10. Tres Pasos Slope Sandstone Bodies, Cerro Divisadero
Authors: Romans B.W. , Hubbard S.M. , Graham S.A. 
Published: April 2015

Abstract
Outcrop accessibility: extremely difficult Outcrop Coordinates: 50.7048°S, 72.7361°W Refer to outcrop 10 on location map
The Tres Pasos Formation (1000–1500 m thick) records the transition from bathyal water depths of the upper part of the Cerro Toro Formation to the shallow-marine and deltaic facies of the overlying Dorotea Formation. The lower part of the Tres Pasos Formation exposed at Cerro Divisadero (600 m thick) is the northernmost (most landward) of the Tres Pasos outcrop locations in this guidebook. Four sandstone-rich packages that range in thickness from 20 to 80 m are recognized and mapped across a ~3 km long outcrop transect. The north-south trending outcrop is generally parallel to depositional dip (basinward to the south), although ridge-and-gully topography provides three-dimensionality at a smaller scale (10s to 100s of meters). The four sandstone-rich units are separated by intervals of shale and siltstone tens of meters thick. Unit 1 is partially covered and minor post-depositional structure (reverse faults and associated drag folds) disrupt detailed architectural characterization of Unit 4. Units 2 and 3 are, therefore, the focus of the panels in this guidebook. Refer to Romans et al. (2008) for detailed presentation and interpretation of the Tres Pasos Formation at Cerro Divisadero.