bluuebunny/crossref_metadata_2025_split huggingface dataset:
Descriptions of Field Trip Stops 1, 2, and 3
Authors: Bate Matthew A. 
Published: April 2015

Abstract
Coalinga Oil Field (Fig. 11) has been oil and gas productive from the Temblor Formation on Coalinga anticline and the contiguous homocline to the southeast since the early part of this century. Oil was first discovered in 1890 in the Oil City area in Upper Cretaceous strata, up-plunge from the present Coalinga Field (Anderson, 1952). Development of the Eastside and Westside Fields began in 1900 and 1901 respectively, close to the Oil City area, but soon spread north, south, and southeast to the limits of the field (Anderson, 1952). The producing area is divided into the Eastside Field on the crest and flanks of the plunging anticline, and the Westside Field along the homocline into the apex of the Coalinga syncline (Kaplow, 1945). Approximately 98% of oil production in the Coalinga Oil Field is from the Temblor Formation (Cal. Oil and Gas Fields, Maps and Data Sheets, 1960), although recent efforts have been directed toward the shallower Etchegoin Formation (Taschman, 1982).
Trapping is accomplished by a combination of structural and strati graphic mechanisms. The structural configuration of Coalinga anticline and its position up-dip from the Buttonwillow depocenter through much of the Tertiary (Zieglar and Spotts, 1978) resulted in migration of oil to the Coalinga Field. Zieglar and Spotts (1978) suggested that hydrocarbon generation occurred in Tertiary beds of the depocenter within the last few million years (perhaps 5 m.y.), but other structures “competing” for the oil, such as the Kettleman Hills, only developed during the Pleistocene episode of folding (Harding, 1976). The Temblor is overlapped by the Monterey and Etchegoin Formations along the Westside Field and is not exposed.
Stratigraphic and Structural Significance of Foliate Serpentinite
Breccias, Wilbur Springs
Authors: Carlson Christine 
Published: April 2015

Abstract
The local appearance of voluminous, monomineralic, foliate serpentinite breccias in the Wilbur Springs section of the Great Valley Sequence record a direct sedimentological response to a late Neocomian accretion event in the Coast Ranges. Field and petrologic studies establish the following events: 1) Early Cretaceous emplacement of lower plate Franciscan rocks (Indian Valley terrane) beneath the proto-Coast Range thrust, 2) deformation of both upper and lower plate rocks into the southeast plunging Wilbur Springs anticline, and 3) contemporaneous protrusion of serpentinite breccias.
Recently discovered modern examples of diapiric serpentinite protrusions of similar magnitude from the Mariana arc-trench system suggest many parallel analogies between the tectonics of active forearcs and the late Mesozoic of the California margin.
Two modes of occurrence of serpentinite have been recognized in the Wilbur Springs area. The first type, serpentinite derived from the alteration of ultramafic tectonite, is widely distributed throughout the Coast Ranges (Bailey et al., 1964). Once considered to be altered ultramafic intrusions and included as part of the Franciscan Complex, these serpentinite masses occur as regionally extensive, allochthonous fault slices or fault-bounded mèlange belts, and tend to be preferentially concentrated along or near contacts between the Franciscan complex and the Great Valley Sequence (Fig. 61). Based on the characteristic spatial association of the serpentinite with layered mafic plutonic rocks, submarine basaltic lavas, and pelagic sedimentary sequences, these serpentinized ultramafic rocks are now generally accepted to represent the basal, mantle tectonite of an ophiolite sequence, the Coast Range Ophiolite, upon which the sediments of the Great Valley Sequence were deposited (Bezore, 1969; Bailey et al., 1970; McLaughlin, 1974; Evarts, 1977; Hopson and Frano, 1977; Hopson et al., 1981).
Descriptions of Field Trip Stops 7, 8, and 9
Authors: Carlson Christine 
Published: April 2015

Abstract
The sedimentary serpentinites we will visit are exposed in the southeast plunging Wilbur Springs anticline, where they interfinger with lower Cretaceous turbidites of the Great Valley Sequence. The Wilbur Springs area (Fig. 65) lies astride this anticlinal structure on the western edge of the Sacramento Valley approximately 175 km north of San Francisco (Fig. 61). The area is named for a hot springs resort on Sulfur Creek, which is located upstream from the Lodoga Road connecting Bear Valley with Highway 20. Barren, block-strewn, grass-free slopes or dense brush characterize areas underlain by serpentinite. Outcrops are sparse, and mainly confined to road and stream cuts. However, even in areas of poor exposure, contacts are easily traced in soils and subcrop. Because of the serpentinite, the area is highly suceptible to landslides and soil creep which locally bury or displace contacts.
The main outcrops of sedimentary serpentinite occur near Sulphur and Bear Creeks, south of Wilbur Springs. Here, thick bedded to massive, crudely stratified, foliate serpentinite breccia is the dominant lithologic facies. A quarry on Highway 20 and adjacent roadcuts provide excellent exposures of foliate serpentinite breccia and its stratigraphic relation with Great Valley strata.
Turn out at the large vista point and walk back across the road to examine the sandstone-shale sequence and the foliate serpentinite breccia exposures in the quarry and in roadcuts at either side. Relocation of the highway and backfill of the original quarry cut has removed some of the section and considerably degraded what remains. Nevertheless, the relationships seen here, though now with some difficulty, are significant enough to justify a look.
Depositional Framework of a Triassic Rift Basin
Authors: Gore Pamela J. W. 
Published: April 2015

Abstract
During the Early Mesozoic, tectonic activity caused the breakup and separation of the North American and African continental plates, initiating the opening of the Atlantic Ocean. This process is generally referred to as rifting, but there was a strong component of strike-slip movement associated with transform faults (Manspeizer, 1981). Wrench-faulting (Bain, 1977) led to the formation of a series of rhomb-shaped half-grabens or pull-apart basins in eastern North America, which filled with continental sediments during the Late Triassic and Early Jurassic. The distribution of sediments within these basins was strongly controlled by tectonic setting. Coarse clastics were deposited in alluvial fans adjacent to faulted basin margins, and broad alluvial plains developed across the basins. Fine-grained, organic-rich sediments accumulated in large lakes, where subsidence was greatest. Deltas formed where rivers entered the lakes, and coal swamps were present locally in some of the basins. In some basins, subaqueous fissure flows of tholeiitic basalt erupted during the Jurassic. Early Mesozoic fault-bounded basins extend from Nova Scotia to southern Georgia, and are referred to as the Newark rift system. Twenty basins are exposed (Figure 1), and the others are buried beneath post-Jurassic sediments of the Atlantic and Gulf coastal plains, and continental shelf. The rocks in the exposed basins belong to the Newark Supergroup; those in the subsurface are generally considered to be coeval, but they are poorly understood, and apparently of diverse lithology, age and origin (Froelich and Olsen, 1984, 1985). The Deep River basin is the southernmost of the exposed rift
Fuel-Grade Peat Deposits of Eastern North Carolina
Authors: Ingram Roy L. , Barnes J. Steve 
Published: April 2015

Abstract
Peat deposits of North Carolina are of three main geologic types that represent accumulations of organic matter in: (1) coastal swamps or pocosins broad, shallow depressions on stream-dissected emerged sea floor, (2) river flood plains, and 3) Carolina bays - elliptical depressions of unknown origin.
The largest deposits of fuel-grade peat (peat with less than 25% ash) are found in coastal swamps pocosins and are: (1) Pamlimarle peninsula, which has 583 sq mi of peatland with 278 million tons of moisture-free peat (1510 sq km, 252 million metric tons), (2) Dismal Swamp, which has 120 sq mi of peatland and 68 million tons of peat (311 sq km, 62 million metric tons), and (3) Croatan Forest, which has 55 sq mi of peatland and 27 million tons of peat 142 sq km, 24 million metric tons). The thickness peat in these deposits normally ranges from 1 to ft (0.3 to 2.4 m) with an average of about 5 ft 1.5 m).
River flood plain peats of unknown extent and quantity occur as lenses in alluvial sands and clays. The ash content is usually high, averaging about 11%.
Of the approximately 500 Carolina bays larger than 100 acres (40 ha), 96 contain some peat. The largest single deposit contains 1.3 million tons of peat under 1,400 acres (1.2 million metric tons under 740 ha).
Most peats are black, fine-grained, and highly decomposed with ash contents commonly less than 5%. Sulfur contents are low (median 0.2%) and heating values are high (median 10,100 ati/lb, or 23.5 MJ/kg).
North Carolina has an estimated 1,060 sq mi (2,740 sq km) of peatland containing about 500 million tons (450 million metric tons) of moisture-free peat.
Tectonic Setting of the Magallanes Basin, Chile
Authors: Fildani A. , Romans B.W. , Hubbard S.M. , Fosdick J.C. 
Published: April 2015

Abstract
The Magallanes Basin is a retroarc foreland basin (Suarez and Pettigrew, 1976; Dalziel, 1981; Wilson, 1991: Fildani and Hessler, 2005) and the sedimentary sequence preserved in the Andean fold-thrust belt reflects the early extensional phase of basin evolution and the subsequent contractile phase with eventual uplift associated with Andean orogenesis (Figs. i.1 and i.2). In the latest Jurassic, extension associated with the initial breakup of southern Gondwana (Bruhn, et al., 1978; Gust, et al., 1985; Pankurst, et al., 2000; Calderón et al., 2007) culminated in the development of an oceanic backarc basin referred to as the Rocas Verdes Basin (Katz, 1963). Ophiolitic rocks exposed in the Cordillera Sarmiento, south and west of Parque Nacional Torres del Paine, represent the obducted remains of the floor of this backarc basin (Wilson, 1991; Fildani and Hessler, 2005; Calderón et al., 2007).
Compression associated with the onset of the Andean orogeny resulted in rapid uplift along the western basin margin and concurrent foreland subsidence. A deep-water depositional phase, caused by flexural loading of obducted ophiolitic blocks over the attenuated crust, is marked by the turbidites of the Punta Barrosa Formation (Fig. i.1). The overlying shale-rich Upper Cretaceous Cerro Toro Formation represents the climax of deep-water sedimentation. Conglomerate-filled channel systems (channel belt up to 8 km wide) within the Cerro Toro Formation developed along much
Outcrop 3. Punta Barrosa Formation Sheet Complex, Headquarters’ Cliff
Authors: Fildani A. 
Published: April 2015

Abstract
Outcrop accessibility: easy Outcrop Coordinates: 51.1786°S, 72.9618°W Refer to outcrop 3 on location map
The Headquarters section (Fig. 3.1A), located within a few hundred meters of the Torres del Paine Park Headquarters, is one of the most accessible outcrops of the upper Punta Barrosa Formation. Stratigraphically, it sits directly below the first mudstone considered as part of the Cerro Toro Formation. This outcrop does not offer the same lateral continuity of exposure as the Marina’s cliff sections, but it presents an interesting packaging of slurry beds (S1) capped by amalgamated thick-bedded conventional turbidites.
In the lower part of the section, the stratigraphic packaging consists of an alternation of thin-bedded fine-grained turbidite packets with more resistant and massive slurry-bed packets. Thin-bedded turbidites include Tc,d,e intervals ranging in thickness from a few centimeters to a maximum of a few tens of centimeters. Slurry bed packets display well-developed meso- and macro-banding. No other sedimentary structures have been observed beyond rare climbing ripples in some of the fine-grained tops of sedimentation units. The lowest bed of the lowest slurry flow package is characterized by a superb example of multi-banding (Fig. 3.1B). It shows fourteen bands defined by dark and light coloration, and it is capped by a 5 cm thick ripple-laminated, fine-grained sandstone interval probably related to more typical turbiditic sedimentation. The top of the stratigraphic succession is capped by amalgamated, thick-bedded high-density turbidity current deposits stacked offset of one another (compensational stacking).
Outcrop 13. Tres Pasos Formation Slope Minibasin Fill, El Chingue Bluff
Authors: Shultz M.R. , Hubbard S.M. 
Published: April 2015

Abstract
Outcrop accessibility: moderate Outcrop Coordinates: 51.1537°S, 72.4725°W Refer to outcrop 13 on location map
Limited exposures of sandstone are present in the Tres Pasos Formation between Sierra Contreras and Laguna Figueroa; an important exception is a 60 m thick succession dominated by coarse-grained turbiditic units at El Chingue Bluff. The stratigraphic section is characterized by an upward coarsening of grain size, and the vertical progression of facies indicating increasing energy. The top of the bluff is defined by the thick sandstone package; beds at the base of this sandstone package are truncated by a normal fault at the southern end of the outcrop, and lap out towards the north onto the tilted hanging wall. Stratal thickening and thinning across the fault, and unfaulted overlying deposits, have led to the interpretation that the fault was active during sand deposition (a growth fault), and that it created accommodation space for the partially ponded sand body (Shultz and Hubbard, 2005). This, and other growth faults in the underlying strata, have contributed to the development of an intraslope minibasin model for deposition. The sandstone package is overlain by a thick succession of mass transport deposits, recording the progradation of the slope across the area. Sandstone dikes are extensive, paralleling growth fault planes. Shultz (2004) has speculated that these dikes were injected downwards, sourced from the coarse sandstone present in the top of the measured section.
Outcrop 14. Tres Pasos Formation Slope Complex, Sierra Dorotea Outcrop Belt
Authors: Hubbard S.M. , Fildani A. 
Published: April 2015

Abstract
Outcrop accessibility: easy to moderate Outcrop Coordinates: 51.3696°S, 72.4210°W Refer to outcrop 14 on location map
A thick sandstone package (~350 m) characterizes the Tres Pasos Formation outcrop between Laguna Figueroa and Arroyo Picana along the Puerto Natales-Cerro Castillo highway (Fig. 14.1). Overlying this sandstone package is a succession of mudstone-dominated strata on the order of 1000 m thick. Sierra Dorotea is capped by deltaic deposits of the Dorotea Formation. In the satellite image presented in Figure 14.1, the northern part of Sierra Dorotea, Cerro Sol and Cerro Cazador are featured. The interpreted stratigraphic architecture consists of large-scale slope surfaces (Chingue, Figueroa, and Puma) building southward (the image is oriented along depositional dip). Sandstones of the Tres Pasos Formation at Laguna Figueroa are interpreted as base-of-slope deposits. Conversely, the corresponding topset units are attributed to the shallow-marine Dorotea Formation. Individual slope surfaces are locally identified as resistant ridges in the satellite image (surface length ~30–35 km; surface stratigraphic relief ~1600 m; slope angle ~2.5–3 degrees). A schematic diagram of the architecture in the region is presented in Figure 14.3, incorporating the location of the El Chingue Bluff slope minibasin fill within the regional context (Outcrop 13).
Architectural elements along the lower part of slope surfaces include mud clast-filled bypass channels, channelized sheets and sandstone-filled channels, featured on the following pages.
Using Accelerometer and Gyroscopic Measures to Quantify Postural Stability
Authors: Alberts Jay L. , Hirsch Joshua R. , Koop Mandy Miller , Schindler David D. , Kana Daniel E. , Linder Susan M. , Campbell Scott , Thota Anil K. 
Published: April 2015

Context
Force platforms and 3-dimensional motion-capture systems provide an accurate method of quantifying postural stability. Substantial cost, space, time to administer, and need for trained personnel limit widespread use of biomechanical techniques in the assessment of postural stability in clinical or field environments.

Objective
To determine whether accelerometer and gyroscope data sampled from a consumer electronics device (iPad2) provide sufficient resolution of center-of-gravity (COG) movements to accurately quantify postural stability in healthy young people.

Design
Controlled laboratory study.

Setting
Research laboratory in an academic medical center.

Patients or Other Participants
A total of 49 healthy individuals (age = 19.5 ± 3.1 years, height = 167.7 ± 13.2 cm, mass = 68.5 ± 17.5 kg).

Intervention(s)
Participants completed the NeuroCom Sensory Organization Test (SOT) with an iPad2 affixed at the sacral level.

Main Outcome Measure(s)
Primary outcomes were equilibrium scores from both systems and the time series of the angular displacement of the anteroposterior COG sway during each trial. A Bland-Altman assessment for agreement was used to compare equilibrium scores produced by the NeuroCom and iPad2 devices. Limits of agreement was defined as the mean bias (NeuroCom − iPad) ± 2 standard deviations. Mean absolute percentage error and median difference between the NeuroCom and iPad2 measurements were used to evaluate how closely the real-time COG sway measured by the 2 systems tracked each other.

Results
The limits between the 2 devices ranged from −0.5° to 0.5° in SOT condition 1 to −2.9° to 1.3° in SOT condition 5. The largest absolute value of the measurement error within the 95% confidence intervals for all conditions was 2.9°. The mean absolute percentage error analysis indicated that the iPad2 tracked NeuroCom COG with an average error ranging from 5.87% to 10.42% of the NeuroCom measurement across SOT conditions.

Conclusions
The iPad2 hardware provided data of sufficient precision and accuracy to quantify postural stability. Accuracy, portability, and affordability make using the iPad2 a reasonable approach for assessing postural stability in clinical and field environments.
Predicting Medical School and Internship Success: Does the Quality of the Research and Clinical Experience Matter?
Authors: Paolino Nathalie D. , Artino Anthony R. , Saguil Aaron , Dong Ting , Durning Steven J. , DeZee Kent J. 
Published: April 2015

ABSTRACT
Objectives: This article explores specific aspects of self-reported clinical and research experience and their relationship to performance in medical training. Methods: This is a retrospective cohort study conducted at the Uniformed Services University. The American Medical College Application Service application was used to discern students' self-reported clinical and research experience. Two authors applied a classification scheme for clinical and research experience to the self-reported experiences. Study outcomes included medical school grade point average (GPA), U.S. Medical Licensing Examination (USMLE) scores, and intern expertise and professionalism scores. A linear regression analysis was conducted for each outcome while controlling for prematriculation GPA. Results: Data were retrieved on 1,020 matriculants. There were several statistically significant but small differences across outcomes when comparing the various categories of clinical experience with no clinical experience. The technician-level experience group had a decrease of 0.1 in cumulative GPA in comparison to students without self-reported clinical experience (p = 0.004). This group also performed 5 points lower on the USMLE Step 2 than students who did not report clinical experience (p = 0.013). The various levels of self-reported research experience were unrelated to success in medical school and graduate medical education. Discussion: These findings indicate that self-reported technician-level clinical experience is related to a small reduction in typically reported outcomes in medical school.
New estimates of tropical mean temperature trend profiles from zonal mean historical radiosonde and pilot balloon wind shear observations
Authors: Pralungo Lorenzo Ramella , Haimberger Leopold 
Published: April 2015

AbstractEstimation of global scale trends and low‐frequency variability directly from radiosonde temperature records is challenging particularly in the Tropics due to large biases in the earlier parts of the records that need to be adjusted. Zonal mean zonal winds and wind shear observations are less prone to time varying biases. Together with a zonal mean reference temperature trend profile in the extratropics, the wind data can be used to estimate zonal mean temperature trends in the tropics using the thermal wind relationship. Earlier estimates using this approach for the periods 1970–2005 and 1979–2005 showed strong trend amplification in the tropical upper troposphere but also very large uncertainties because the latitude for the reference profile was chosen very far north and due to a lack of data in the tropics.Both sources of uncertainties have been addressed by (i) using reference temperature profiles from homogenized radiosonde temperature data sets, (ii) using the new Global historical Radiosondes and Tracked Balloons Archive on standard pressure levels (GRASP) as data source that includes not only radiosondes but also pilot balloons, and (iii) more accurate vertical discretization and sampling of wind data. The new trend estimates are extended back to 1958 and are considerably less noisy. Trend amplification factors between 1.3 and 2.6 were found in the intervals 1979–2005 and 1958–2010, respectively, when using wind shear information. The best estimates for the warming maxima in the upper tropical troposphere agree well with those directly from temperatures but tend to be located at higher altitudes.
Three‐dimensional versus two‐dimensional bed form‐induced hyporheic exchange
Authors: Chen Xiaobing , Cardenas M. Bayani , Chen Li 
Published: April 2015

AbstractThe hyporheic zone is often a critical component of river systems. Hyporheic exchange is generally forced by variation in riverbed topography such as due to bed forms. Most previous research on bed form‐driven hyporheic flow has focused on two‐dimensional (2‐D) dunes and ripples, while little has been done on their three‐dimensional (3‐D) counterparts. Here we compared hyporheic exchange and associated metrics for a previously studied pair of corresponding 2‐D and 3‐D bed forms. To accomplish this, a series of multiphysics computational fluid dynamics models were conducted both in 2‐D and 3‐D with similar open channel Reynolds numbers (Re). Results show that the pressure gradient along the sediment‐water interface is highly sensitive to the spatial structure of bed forms, which consequently determines hyporheic flow dynamics. Hyporheic flux is a function of Re for both 2‐D and 3‐D dunes via a power law; however, the equivalent 3‐D dunes have a higher flux since the 3‐D form induces more drag. The hyporheic zone depths and volumes are only slightly different with the 3‐D case having a larger volume. The mean fluid residence times for both cases are related to Re by an inverse power law relationship, with the 3‐D dune having smaller residence times at moderate to high Re. The effects of increasing flux on residence time in 3‐D dunes are partly modulated by a slightly increasing hyporheic volume. Our results suggest that a 2‐D idealization is a reasonable approximation for the more complex 3‐D situation if local details are unimportant but that development of predictive models for mean fluxes and residence times, which are critical for biogeochemical processes, based on 2‐D models may be insufficient.