bluuebunny/crossref_metadata_2025 huggingface dataset:
Detailed Heat/Mass Transfer Distributions in a Rotating Smooth Channel With Bleed Flow
Authors: Kim Kyung Min , Kim Sang In , Jeon Yun Heung , Lee Dong Hyun , Cho Hyung Hee
Published: November 2007

In this study, the effects of bleed flow on heat/mass transfer in a rotating smooth square channel were investigated. The hydraulic diameter (Dh) of the channel was 40.0mm, and the diameter of the bleed holes (d) on the leading surface was 4.5mm. Tests were conducted under various bleed flow rates (0%, 10%, 20%) and rotation numbers (0, 0.2, 0.4), while the Reynolds number was fixed at 10,000. A naphthalene sublimation method was employed to determine the detailed heat transfer coefficients using a heat and mass transfer analogy. The results suggested heat/mass transfer characteristics in the internal cooling passage to be influenced by tripping flow as well as Coriolis force induced by bleed flow and channel rotation. In cases influenced by bleed flow, the heat/mass transfer on the leading surface was higher than that without bleed flow. The heat/mass transfer on the leading surface increased with the number of rotations to Ro=0.2, after which it decreased due to rotation effects.
Flow, Thermal, Energy Transfer, and Entropy Generation Characteristics Inside Wavy Enclosures Filled With Microstructures
Authors: Mahmud Shohel , Fraser Roydon Andrew , Pop Ioan
Published: November 2007

Flow, thermal, energy, and irreversibility characteristics inside wavy enclosures packed with microstructures are reported in this paper. It is assumed that the entire enclosure has sufficient and interconnected void spaces; those allow fluid movement inside the cavity. The Darcy momentum equation is selected for momentum transfer modeling by considering a relatively small pore Reynolds number (Rep). Modeled equations are solved numerically using the finite volume method. Streamlines, isothermal lines, energy streamlines, average Nusselt number, and average entropy generation number are calculated and displayed in order to show their dependency on and variation with Rayleigh number (Ra), surface waviness (λ), and aspect ratio (AR) of the enclosure. Depending on the wall waviness pattern, the enclosure is divided into three modes (phase-plus, phase-zero, and phase-minus modes). However, for the current calculation, wall waviness is kept symmetric with respect to the vertical and horizontal centerlines of the enclosure.
A General Scheme for the Boundary Conditions in Convective and Diffusive Heat Transfer With Immersed Boundary Methods
Authors: Pacheco-Vega Arturo , Pacheco J. Rafael , Rodić Tamara
Published: November 2007

We describe the implementation of an interpolation technique, which allows the accurate imposition of the Dirichlet, Neumann, and mixed (Robin) boundary conditions on complex geometries using the immersed-boundary technique on Cartesian grids, where the interface effects are transmitted through forcing functions. The scheme is general in that it does not involve any special treatment to handle either one of the three types of boundary conditions. The accuracy of the interpolation algorithm on the boundary is assessed using several two- and three-dimensional heat transfer problems: (1) forced convection over cylinders placed in an unbounded flow, (2) natural convection on a cylinder placed inside a cavity, (3) heat diffusion inside an annulus, and (4) forced convection around a stationary sphere. The results show that the scheme preserves the second-order accuracy of the equations solver and are in agreement with analytical and/or numerical data.
A Convection Heat Transfer Correlation for a Binary Air-Helium Mixture at Low Reynolds Number
Authors: Banerjee Arindam , Andrews Malcolm J.
Published: November 2007

The results of experiments investigating heat transfer from a hot wire in a binary mixture of air and helium are reported. The measurements were made with a constant temperature anemometer at low Reynolds numbers (0.25<Re<1.2) and correlated by treating the data in terms of a suitably defined Reynolds and Nusselt numbers based on the wire diameter. The correlation was obtained by taking into account the temperature dependency of gas properties, properties of binary gas mixtures, and the fluid slip at the probe surfaces as well as gas accommodation effects. The correlation has been used to measure velocity and velocity-density statistics across a buoyancy driven Rayleigh–Taylor mixing layer with a hot wire. The measured values obtained with the correlation agree well with measurements obtained with a more rigorous and extensive calibration technique (at two different overheat ratios). The reported correlation technique can be used as a faster and less expensive method for calibrating hot wires in binary gas mixtures.
Transition Boiling Heat Transfer of Droplet Streams and Sprays
Authors: Bernardin John D. , Mudawar Issam
Published: November 2007

An experimental study was performed to characterize the transition boiling heat transfer rate from a surface to a stream of impinging water droplets and to extrapolate this information to predict the transition boiling heat transfer of a dilute spray. First, transition boiling heat transfer data were gathered for a continuous stream of monodispersed water droplets striking a polished nickel surface. From these data, empirical correlations were developed to describe the heat transfer rate and heat transfer efficiency for droplet velocities between 1.0ms−1 and 7.1ms−1, droplet diameters ranging from 0.250×10−3mto1.002×10−3m, and surface temperatures covering 110–240°C. By properly accounting for the hydrodynamic differences between a spray and a single droplet stream, the empirical single droplet stream heat transfer correlations were effectively extrapolated into a model for predicting the transition boiling heat flux of dilute sprays (Q″≈0.5×10−3m3s−1m−2).
Heat Transfer Enhancement for Turbulent Flow Through Blockages With Round and Elongated Holes in a Rectangular Channel
Authors: Ahn H. S. , Lee S. W. , Lau S. C.
Published: November 2007

Experiments were conducted to determine the average heat transfer coefficients on three wall segments between blockages with holes in a wide rectangular channel. Eight different configurations of the holes in the blockages—two diameters and four aspect ratios of the holes—were examined. The pressure drops across the blockages were also measured. The results showed that the elongated holes in the blockages in this study enhanced more heat transfer than the round holes, but they also caused larger pressure drops across the blockages.
Vortex flow generated by a magnetic stirrer
Authors: Halász Gábor , Gyüre Balázs , Jánosi Imre M. , Szabó K. Gábor , Tél Tamás
Published: November 2007

We investigate the flow generated by a magnetic stirrer in cylindrical containers by optical observations, particle image velocimetry measurements, and particle and dye tracking methods. The tangential flow is that of an ideal vortex outside a core, but inside downwelling occurs with a strong jet in the very middle. In the core region dye patterns remain visible over minutes indicating inefficient mixing in this region. The results of quantitative measurements can be described by simple relations that depend on the stirring bar’s rotation frequency. The tangential flow is similar to that of large atmospheric vortices such as dust devils and tornadoes.
Thermodynamics of a pure substance at the triple point
Authors: Velasco S. , Fernández-Pineda C.
Published: November 2007

A thermodynamic study of a pure substance at the triple point is presented. In particular, we show that the mass fractions of the phases coexisting at the triple point obey lever rules in the specific entropy-specific volume diagram, and the relative changes in the mass fractions present in each phase along reversible isochoric and adiabatic processes of a pure substance at the triple point are governed by the relative sizes of the segments of the triple-point line in the pressure-specific volume diagram and in the temperature-specific entropy diagram. Applications to the ordinary triple point of water and to the triple point of Al2SiO5 polymorphs are presented.
An experimental study of Wiffle ball aerodynamics
Authors: Rossmann Jenn , Rau Andrew
Published: November 2007

We measure the aerodynamic forces on a Wiffle ball as a function of the Reynolds number and ball orientation. The effects of asymmetric flow outside the ball and flow within the ball are considered, and are both associated with the ball’s tendency to curve without pitcher-imparted spin. The problem of Wiffle ball aerodynamics is an accessible way to introduce topics such as boundary layer separation and transition to turbulence.
Experimental study of the frequency repulsion effect
Authors: Gamarra R. F. , Josebachuili M. , Zurita P. , Gil S.
Published: November 2007

We discuss an experiment on coupled RLC circuits with variable coupling strength. The inductive coupling can be easily varied and measured for different configurations. The experiment allows us to explore the variation of the resonance frequencies as a function of the coupling strength between the oscillators. The system illustrates the effect of eigenfrequency repulsion when an interaction couples different modes of oscillation. The experiment is conceptually simple, and its results can be compared quantitatively with theoretical predictions.
Identification of Immunologic and Pathologic Parameters of Death versus Survival in Respiratory Tularemia
Authors: Chiavolini Damiana , Alroy Joseph , King Carol A. , Jorth Peter , Weir Susan , Madico Guillermo , Murphy John R. , Wetzler Lee M.
Published: November 2007

Francisella tularensiscan cause severe disseminated disease after respiratory infection. The identification of factors involved in mortality or recovery following induction of tularemia in the mouse will improve our understanding of the natural history of this disease and facilitate future evaluation of vaccine candidate preparations. BALB/c mice were infected intranasally with the live vaccine strain (LVS) ofF. tularensissubsp.holarcticaand euthanized at different stages of disease to analyze the induction of immune molecules, gross anatomical features of organs, bacterial burdens, and progression of the histopathological changes in lung and spleen. Tissue-specific interleukin-6 (IL-6), macrophage inflammatory protein 2, and monocyte chemotactic protein 1 were immune markers of mortality, while anti-LVS immunoglobulin M and IL-1β were associated with survival. Moribund mice had enlarged spleens and lungs, while surviving mice had even more prominent splenomegaly and normal-appearing lungs. Histopathology of the spleens of severely ill mice was characterized by disrupted lymphoid follicles and fragmented nuclei, while the spleens of survivors appeared healthy but with increased numbers of megakaryocytes and erythrocytes. Histopathology of the lungs of severely ill mice indicated severe pneumonia. Lungs of survivors at early time points showed increased inflammation, while at late times they appeared healthy with peribronchial lymphoid aggregates. Our results suggest that host immune factors are able to affect bacterial dissemination after respiratory tularemia, provide new insights regarding the pathological characteristics of pulmonary tularemia leading to systemic disease, and potentially identify immune markers associated with recovery from the disease.
Genomic Comparison of Virulent
Rickettsia rickettsii
Sheila Smith and Avirulent
Rickettsia rickettsii
Iowa
Authors: Ellison Damon W. , Clark Tina R. , Sturdevant Daniel E. , Virtaneva Kimmo , Porcella Stephen F. , Hackstadt Ted
Published: November 2007

Rickettsia rickettsii
is an obligate intracellular pathogen that is the causative agent of Rocky Mountain spotted fever. To identify genes involved in the virulence of
R. rickettsii
, the genome of an avirulent strain,
R. rickettsii
Iowa, was sequenced and compared to the genome of the virulent strain
R. rickettsii
Sheila Smith.
R. rickettsii
Iowa is avirulent in a guinea pig model of infection and displays altered plaque morphology with decreased lysis of infected host cells. Comparison of the two genomes revealed that
R. rickettsii
Iowa and
R. rickettsii
Sheila Smith share a high degree of sequence identity. A whole-genome alignment comparing
R. rickettsii
Iowa to
R. rickettsii
Sheila Smith revealed a total of 143 deletions for the two strains. A subsequent single-nucleotide polymorphism (SNP) analysis comparing Iowa to Sheila Smith revealed 492 SNPs for the two genomes. One of the deletions in
R. rickettsii
Iowa truncates
rompA
, encoding a major surface antigen (rickettsial outer membrane protein A [rOmpA]) and member of the autotransporter family, 660 bp from the start of translation. Immunoblotting and immunofluorescence confirmed the absence of rOmpA from
R. rickettsii
Iowa. In addition,
R. rickettsii
Iowa is defective in the processing of rOmpB, an autotransporter and also a major surface antigen of spotted fever group rickettsiae. Disruption of
rompA
and the defect in rOmpB processing are most likely factors that contribute to the avirulence of
R. rickettsii
Iowa. Genomic differences between the two strains do not significantly alter gene expression as analysis of microarrays revealed only four differences in gene expression between
R. rickettsii
Iowa and
R. rickettsii
strain R. Although
R. rickettsii
Iowa does not cause apparent disease, infection of guinea pigs with this strain confers protection against subsequent challenge with the virulent strain
R. rickettsii
Sheila Smith.
Resistance of
Yersinia pestis
to Complement-Dependent Killing Is Mediated by the Ail Outer Membrane Protein
Authors: Bartra Sara Schesser , Styer Katie L. , O'Bryant Deanna M. , Nilles Matthew L. , Hinnebusch B. Joseph , Aballay Alejandro , Plano Gregory V.
Published: November 2007

Yersinia pestis
, the causative agent of plague, must survive in blood in order to cause disease and to be transmitted from host to host by fleas. Members of the Ail/Lom family of outer membrane proteins provide protection from complement-dependent killing for a number of pathogenic bacteria. The
Y. pestis
KIM genome is predicted to encode four Ail/Lom family proteins.
Y. pestis
mutants specifically deficient in expression of each of these proteins were constructed using lambda Red-mediated recombination. The Ail outer membrane protein was essential for
Y. pestis
to resist complement-mediated killing at 26 and 37°C. Ail was expressed at high levels at both 26 and 37°C, but not at 6°C. Expression of Ail in
Escherichia coli
provided protection from the bactericidal activity of complement. High-level expression of the three other
Y. pestis
Ail/Lom family proteins (the y1682, y2034, and y2446 proteins) provided no protection against complement-mediated bacterial killing. A
Y. pestis ail
deletion mutant was rapidly killed by sera obtained from all mammals tested except mouse serum. The role of Ail in infection of mice,
Caenorhabditis elegans
, and fleas was investigated.
Waimea Canyon, Kauai, Hawaii
Authors: Clague David A. , Bohrson Wendy
Published: November 2007

Kauai is the westernmost of the principal Hawaiian Islands. Figure 1 shows the road guide to Waimea Canyon starting in the town of Kekaha and ending in the town of Waimea. The entire trip can be made in a passenger car, with the exception of the optional hike down the Kukui trail. The road stops are at major viewpoints that have parking areas and facilities. Do not reverse the order of the starting and stopping points, since the road between the town of Waimea and the intersection of Waimea Canyon Road and Hawaii 55 is so steep that small passenger cars may overheat going uphill. The entire roadlog is just over 40 mi (64 km) long and can be completed in about 3 hours, including relatively brief stops; allow more time for longer stops. The starting point in the town of Kekaha is roughly 45 mi (72 km) and 1 hour from Lihue. The optional hike down the Kukui trail to the floor of Waimea Canyon can be completed in about 3 to 4 hours; the trail is steep, strenuous, and slippery when wet. Those interested in the hike may wish to spend a full day to allow time to explore the canyon floor.
Kilauea caldera and adjoining volcanic rift zones
Authors: Hazlett Richard W.
Published: November 2007

Kilauea volcano is located at the southeastern corner of the Island of Hawaii (Fig. 1). Access to the site is easy by ordinary passenger vehicle. Major mainland and interisland airlines serve island airports, where numerous car rental agencies are located. Because Hawaii is a popular tourist destination, it is recommended that car reservations be placed well in advance of a visit. Hawaii 11 links Hilo, the largest town on the island, directly with the Kilauea summit area, a drive of about 31 mi (50 km). A map and information concerning the status of roads and trails within Hawaii Volcanoes National Park may be obtained at the Kilauea Visitor Center, a short side trip from Hawaii 11 (Fig. 2). The Visitor Center is a good place for one to begin exploring the caldera area.
Late Quaternary fault scarp at Lone Pine, California; Location of oblique slip during the great 1872 earthquake and earlier earthquakes
Authors: Lubetkin Lester K. C. , Clark Malcolm M.
Published: November 2007

To reach this site, drive west on Whitney Portal Road about 0.7 mi (1.2 km) from U.S. Highway 395 in the center of Lone Pine (Fig. 1). About 0.15 mi (0.2 km) west of the Los Angeles Aqueduct, park in the pavedarea northof the road. Walk north and then northeast about 0.3 mi (0.5 km) along the dirt roads that lead to the area just east of the main scarp.
Papoose Flat pluton, Inyo Mountains, California
Authors: Nelson C. A.
Published: November 2007

Papoose Flat pluton, a late Cretaceus (75–81 Ma) granitic body in the Inyo Mountains, California, is one of several Mesozoic intrusive in the White-Inyo Range that are “satellites” of the large Sierra batholith to the west. The western portion of the pluton can be reached by way of the Hines Road (Waucoba Mountain 15-minute Quadrangle) (Fig. 1, insert); the eastern exposures by way of the Waucoba Road leading to Saline Valley (Waucoba Spring and Waucoba Wash 15-minute quadrangles). The published geologic maps of thesequadrangles (Nelson, 1966, 1971; Ross, 1967) and the geologic map of the pluton (Nelson and others, 1978) are important adjuncts to this report. Only the HinesRoad requires a four-wheel drive vehicle.
Long Valley caldera, eastern California
Authors: Bailey Roy A.
Published: November 2007

Long Valley caldera (Fig. 1) is in eastern California, attheeastern base of the Sierra Nevada between Mono Lake andOwens Valley. Traversed by U.S. 395, the caldera is about 310 mi (500 km) north of Los Angeles and 165 mi (265 km)south of Reno. It is midway between the towns of Bishop and LeVining and contains the resort town of Mammoth Lakes.
Late Pleistocene angular unconformity at San Pedro, California
Authors: Yule J. Douglas , Zenger Donald H.
Published: November 2007

This outcrop is located on Second Street between Pacific Avenue and Mesa Street in central San Pedro (Fig.1), approximately 25 mi (40 km) south of downtownLos Angeles, California.To reach the “Second Street locality” from downtown, take the Harbor Freeway (I-1 10) south to its termination at Gaffey Street in San Pedro. Proceed south on Gaffey Street approximately 0.3 mi (0.5 km) to Second Street. Turn left (east) on Second Street and proceed 0.2 mi (0.3 km) to Pacific Avenue.Cross Pacific Avenue and park along Second Street. The outcrop extends along the north side of Second Street for 360ft(110 m)east of the alleyway adjacent to the Tropicana Bakery. (The authors wholeheartedly recommend a visit to this authentic panaderia)
A section through the Peninsular Ranges batholith, Elsinore Mountains, southern California
Authors: Woyski Margaret S. , Howard Astrid H.
Published: November 2007

The Elsinore Mountains in the Cleveland National Forest of southern California are situated in the northwestern Peninsular Ranges. They lie southwest of and overlook Lake Elsinore at elevations of 2,600 to3,600 ft (790 to 1,100 m). The northeastern front of the mountains is a precipitous escarpment that rises 1,350 to 2,350 ft (410 to 720 m) above the lake at its base. The site is reached by taking the Ortega Highway (California 74) from either 1–15 at Lake Elsinore or I-5 at San Juan Capistrano to the Main Divide Truck Trail (Fig.1) where it intersects the Ortega Highway 0.2 mi (0.3 km) west of the summit. Roadcuts along the Main Divide Truck Trail (a graded dirt road) are accessible by passenger car and, with caution, by bus. Two campgrounds are located at the intersection of the Ortega Highway with the Main Divide Truck Trail and group camping sites (limited to 70people) are located just off the West Extension of the Main Divide Truck Trail. Make reservations with the Cleveland National Forest Trabuco District Office, Corona Ranger Station,1147 East Sixth Street, Corona, California 91719, (714) 736–1811. There is a daily charge for all campgrounds.
San Andreas fault, Cajon Pass, southern California
Authors: Weldon Ray J.
Published: November 2007

The field area discussed here straddles 1–15 and old Route66 (here part of U.S. 395) where they cross the TransverseRanges, about 50 mi (80 km) northeast of Los Angeles, California (Fig.1). Most of the sites can be reached by car on paved orgood dirt roads. Sites east of I–15 are accessible only with four-wheel drive or a short walk from a paved road. The land notobviously occupied by structures or surrounded by fences belongsto the Forest Service, the Highway Department, or the railroadsso access does not require special permission.
Hog Back
Authors: Herber Lawrence J.
Published: November 2007

Hog Back, as named on the 7½-minute Mt. Baldy, California, Quadrangle, lies in San Antonio Canyon (NE¼Sec.36, T.2N., R.8W.) in the Angeles National Forest 1.1 mi (1.8 km) south of Mt. Baldy Village (Fig.1). Hog Back appears as a large obstruction nearly choking off the canyon when looking upstream (Fig.2). Looking south from Glendora Ridge Road, it appears as a low, rounded lump in the canyon floor(Fig.3; Shelton, 1966.

Mt. Baldy Road crosses the head of Hog Back, providing easy access, and a roadside parking area suitable for large buses is near the head of the slide mass. A switchback footpath descends from the parking area to the old Mt. Baldy Road (abandoned) excavatedacross the toe of the slide. A l-mi (1.6-km) hike along the footpath, abandoned road, and return to parking area via Mt. Baldy Road yields good cross-sectional views of the toe and head of the slide mass
The San Gabriel anorthosite-syenite-gabbro San Gabriel Mountains, California
Authors: Carter Bruce A
Published: November 2007

The San Gabriel anorthosite-syenite-gabbro body is exposed in the western San Gabriel Mountains about 30 mi (48 km) north of Los Angeles (Fig. 1). The most abundant lithologies of this body, which constitute the anorthosite-leucogabbro unit, are easily accessible via Angeles Forest Highway (N3) along Mill Creek about 18 mi (28.8 km) south of Palmdale (Fig 11, 2A). However, many of the most interesting lithologies of this body can be seen only by driving several mi (km) on U.S. Forest Service roads into he central part of the body west of Angeles Forest Highway. These localities can be reached from Angeles Forest Highway by driving west from Mill Creek Summit, past Mt. Gleason, to North Fork Saddle, and on down Pacoima Canyon. Alternately, they can be reached by driving east either from Santa Clara Divide or from Dillon Divide on the Sand Canyon-Little Tujunga Road (Fig. 1).

A second important group of lithologies constitutes the syenite unit and can be seen near “Sold” on the North Fork Saddle-Magic Mountain-Mount Gleason road (Figs. 1, 2B). This road is usually in good condition and is easily passable by conventional automobile except between December and February, when it is occasionally covered by snow at higher elevations. A third important group of lithologies constitutes the Jotunite unit and can be seen along Pacoima Canyon (Fig. 2C). The road through Pacoima Canyon, reached from either Dillon Divide or North Fork Saddle (Fig, 1), is rough and may require use of a four-wheel-drive vehicle during winter and spring.
Geology of the Devil's Punchbowl, Los Angeles County, California
Authors: Dibblee T.W.
Published: November 2007

The Devil's Punchbowl, now a county park, is a spectacular exposure of Tertiary sandstone strata on the southwest margin of the Mojave Desert adjacent to the San Gabriel Mountains.

This unusual feature is located south of Valyermo Ranger Station, about 7 mi (11 km) southeast of Pearblosso in the Mojave Desert in northern Los Angeles County (Fig. 1). It is between the high San Gabriel Mountains to the south, and lower hills to the north, which hide it from the adjacent Mojave Desert. The Devil's Punchbowl is on and within the north border of the Angeles National Forest. This site is accessible via a paved road (L.A. County Road N6) direct from Pearblossom on California 138.

The Devil's Punchbowl is shown on the Valyermo 7 1/2- and 15-minute Quadrangles. The geology described here is summarized from Dibblee (1967).
The San Andreas fault at Wallace Creek, San Luis Obispo County, California
Authors: Sieh Kerry , Wallace Robert E.
Published: November 2007

From either the coast or the interior, Wallace Creek is most easily reached by way of California 58 (Fig.1). Precisely at the southwestern base of the Temblor Range, leave California 58 and drive southwest onan unmarked paved road about 0.2 mi (0.3 km) to a junction with an unpaved road (Fig.2). Turn left (south) on this road and follow the San Andreas fault to Wallace Creek.The unpaved road leading to Wallace Creekis impassable to all vehicles during and immediately following major storms.At all other times, two-wheel- or four-wheel-drive vehicles can be easily driven to within 1,300 ft (400 m) of the site. To avoid the gradual destruction of fragile tectonic landforms, park vehicles along the road near the section 33/34 boundary fence and walk theshort distance north to the fault. During the dry season, be careful not to park on dry, flammable vegetation.
Paleocene turbidites and modern landslides of the Point San Pedro-Devil’s Slide area, San Mateo County, California
Authors: Nilsen Tor H. , Yount James C.
Published: November 2007

This site is located adjacent to the California coast in northern San Mateo County, about 15 mi (25 km) south-southwest of downtown San Francisco (Fig. 1). From San Francisco, take 1–280 south to its intersection with California 1, then follow California 1 southward for approximately 9 mi (15 km) to San Pedro Avenue in Pacifica. From the central San Francisco Peninsula, take California 92 westward to its intersection with California 1 in Half Moon Bay, then proceed northward on California 1 for approximately 10 mi (16 km) to San Pedro Avenue in Pacifica.

From the southern San Francisco Peninsula or Santa Cruz County, take California 1 north to San Pedro Avenue in Pacifica. The Shelter Cove locality (Stop 1) can be reached by taking San Pedro Avenue west for three blocks from California 1, turning north on Danmann Road, and proceeding two blocks north to Shelter Cove Road. At present (July 1986), Shelter Cove Road is a privately maintained access that has sustained substantial landslide damage and is passable only on foot. The property at Shelter Cove is private, and permission to enter must be obtained from the owners (Telegan Realty, Pacifica, California). Roadcuts along California 1 are located south of San Pedro Avenue. Stop 2 is located 0.7 mi (1.1 km) to the south on the northwest side of the highway. Stop 3 in the Devil’s Slide area is located 0.6 mi (1 km) farther south along California 1 and Stop 4 another 0.7 mi (1.1 km) to the south. Stops 2,3, and 4 are subject to heavy traffic and have limited parking along a narrow, twisting, and dangerous roadway. Exposures are close to the roadway, so great caution should be exercised.
Unconformity between Coast Range ophiolite and part of the lower Great Valley sequence, South Fork of Elder Creek, Tehama County, California
Authors: Blake M.C. , Jayko A.S. , Jones D.L. , Rogers B.W.
Published: November 2007

The South Fork of Elder Creek is located on private property about 6 mi (10 km) northwest of Paskenta, Calif. (Fig. 1). To visit this locality it is necessary to call Mr. Les Sutfin (916-824-4628) and arrange to pick up the key to the gate at his home in Corning. From the Paskenta Store, drive 3.3 mi (5.3 km) north on the Toomes Camp road to the locked gate on the north side of the road. From here, take the Pellows Road (four-wheel drive vehicle recommended) 3.6 mi (5 km) north to the end of the road, then walk west along the trail parallel to the South Fork of Elder Creek for approximately 0.5 mi (0.8 km) to the unconformity(Fig. 2).
Late High Cascade volcanism from summit of McKenzie Pass, Oregon
Authors: Taylor Edward M.
Published: November 2007

The observation platform at Dee Wright viewpoint facility on the summit of McKenzie Pass, Oregon State Highway 242, can be reached by driving east from Eugene, Oregon, 55 mi(89 km) on U.S. 126 then 22 mi (35 km) on Oregon 242 or by driving west from Sisters, Oregon, 15 mi (24 km) on Oregon 242(Fig. 1). The highwayis paved but narrow with sharp curves. The site elevation is 5,300 ft (1,617 m); it is generally closed bysnow November through July.
John Day Fossil Beds National Monument, Oregon
Authors: Robinson Paul T.
Published: November 2007

The Painted Hills unit, formerly Painted Hills State Park, lies along Bridge Creek about 9.5 mi (16 km)northwest of Mitchell, Wheeler County, Oregon, near the intersection of T.1O and 11S. and R.20 and 21E. Itcan be reached by taking the Bridge Creek road north from U.S. 26, which runs between Prineville and Mitchell (Fig. 1). The turnoff is located 4 mi (6.5 km) west of Mitchell and is marked by a sign directing travelers to the Painted Hills. The Bridge Creek road is paved and is passable in all weather by passenger cars.
Evidence for dozens of stupendous floods from Glacial Lake Missoula in eastern Washington, Idaho, and Montana
Authors: Waitt Richard B.
Published: November 2007

Burlingame Canyon (Fig. 1). Walla Walla valley, southeast Washington about 2.5 mi (4 km) south of Lowden. Lat.46° 01' N.; Long. 118°36' W. SW1/4SW1/4Sec.5, T.6N., R.34E. (SW÷ of Lowden, Washington 7 1/2-minute Quadrangle). Drive on U.S. 12 to Lowden, 11 mi (17.7 km) west from Walla Walla,18 mi (29 km) eastfrom Wallula Junction at U.S. 395. From Lowden, drivesouth for 0.25 mi(0.4 km) to intersection; turn south (right) on road to Gardena, and drive south another 2.4 mi (3.9 km) to house on right just beyond crossing of irrigation ditch. Burlingame “canyon” is another 0.1 mi (0.16 km) along road and 200 ft (60 m) west of road. (Please do not try to park or walk in the clear, vaguely fenced area between road and head of canyon; this is man-made in-ground nesting for pollinating bees.)
Columbia River Basalt Group, Joseph and Grande Ronde canyons, Washington
Authors: Reidel S.P. , Hooper P.R. , Price S.M.
Published: November 2007

The Grande Ronde-Joseph Canyon area is located in southeast Washington near the common boundaries of Washington, Oregon, and Idaho (Fig.1). The locality lies within the canyon country which forms the southeast part ofthe Columbia Plateau Province near the eastern termination of the Blue Mountains and the southern boundary of the Lewiston Basin.

The site can be reached by following Washington SR 129 south from Clarkston to Asotin, Washington, and then by following the Snake River road (lst street in Asotin) south from Asotin for 25 mi (40 km) to the confluence of the Snake and Grande Ronde rivers. The Snake River road is paved for the first 13 mi (21 km) but then becomes a well-maintained gravel road that serves the area. All sites are easily reached from this road. Land within the area either is owned by the Washington Department of Game, Fish, and Wildlife Service or is private. Information about current ownership can be obtained from the headquarters of the Chief Joseph Fish and Wildlife area in Joseph Canyon (H, Fig.2). Permission must be obtained to visit private land, but landowners understand the significance of the area and have always granted access graciously.
Ingalls Tectonic Complex and Swauk Formation, Ruby Creek area, Cascade Mountains, Washington
Authors: Johnson Samuel Y. , Miller Robert B.
Published: November 2007

The Ruby Creek area encompasses several outcrops of the Late Jurassic or Early Cretaceus Ingalls Tectonic Complex and the Eocene Swauk Formation in the central Cascades of Washington (Fig.1, Stop 1). To get to the outcrops on Ruby Creek, either: (1) drive south on U.S. 97 (Swauk Pass Highway) from its junction with U.S. 2 for 8.9 mi (14.3 km), or (2) drive north on U.S. 97 from its junction with U.S. 131 for 26.6 mi (42.8 km).Turn east off U.S. 97 onto the well-marked RubyCreek Road(logging road 2322) and park. Walk up the road for several hundred meters across a fault contact between the Ingalls and the Swauk. Locations of other outcrops are shown on Figure 1, and their accesses from the Ruby Creek exposures are described later in the text.
Melange rocks of Washington’s Olympic coast
Authors: Rau Weldon W.
Published: November 2007

One of the most impressive outcrops of melange rocks along the Washington coast is exposed continuously for 2.5 mi (4km) in sea cliffs immediately south of the mouth of Raft River on the Quinault Indian Reservation, Grays Harbor County (Taholah 15-minute quadrangle) (Fig. 1). This site affords a rare opportunity for viewing a rock type that has resulted largely from tectonism and is particulary significant to an understanding of the general geology and tectonic framework of the Olympic Moun is 5 mi (8 km) north of Taholah and is reached by a gravel road. Because it is a beach locality on the Quinault Indian Reservation, permission to walk on the beaches must be obtained from the Quinault Tribal Office in Taholah. Instructions will alsobe given there for the best route from the road to the beach. Several trails are less than 0.25 mi (0,4 km) in length.
The Late Cretaceus San Juan thrust system, Washington
Authors: Brandon Mark T. , Cowan Darrel S.
Published: November 2007

The San Juan Islands are located at the north end of Puget Sound in northwestern Washington State. This field guide in-eludes four localities: one on Lopez Island and three on San Juan Island. To reach the islands (Fig. 1 1), take I–5 to Exit 230, thendrive west on Washington 20 to the Anacortes ferry terminal.Washington State ferries provide frequent daily service for carsand passengers to Lopez and San Juan Islands. Long waits shouldbe expected on summer weekends.
Cache Creek-Ashcroft area, western Intermontane Belt, British Columbia
Authors: Travers William B.
Published: November 2007

Outcrops in and near the settlements of Cache Creek and Ashcroft, southern British Columbia (Fig. 1), provide an opportunity to view some of the structures and rocks that help to explain the evolution and amalgamation of the allochthonous terranes of the southern Canadian Cordillera. Sediments and igneous rocks ofthe Cache Creek and Nicola Groups formed in late Paleozoic to late Triassic times in oceanic and island arc settings. The sediments of the Ashcroft Formation were deposited from Early through Middle Jurassic time in an arc-related basin. In Late Jurassic or possibly earliest Cretaceus time, thrust faulting juxtapose Cache Creek-Nicola rocks over Ashcroft strata. This event is thought to have sutured these terranes to Quesnellia of which the Ashcroft Formation is generally considered to be a part. This faulting may havebeen related to the early (Late Jurassic) deformationin the Omineca Crystalline Belt when east-directed thrust faults joined Quesnellia to that crystalline terrane.
Sedimentology of the Upper Cretaceus Nanaimo Basin, British Columbia
Authors: Pacht Jory A.
Published: November 2007

The Nanaimo Group is an assemblage of conglomerate, sandstone, siltstone, shale, and minor coal deposited in the Nanaimo Basin during Santonian through Maestrichtian time (Muller and Jeletzky, 1970; Ward, 1978). It crops out on southeastern Vancouver Island, the Gulf Islands of British Columbia, and the San Juan Islands of Washington (Figs. 1, 2). Nearly continuous outcrops of the Namaimo Group occur along seacliffs on Vancouver Island, and on the Gulf and San Juan islands. Good exposures are also present along roadcuts and major rivers on Vancouver Island.

Ferries from the mainland to Vancouver Island and most of the Gulf and San Juan islands can be boarded at Anacortes, Washington, and Tawassen, British Columbia, and taken to Sidney, British Columbia (approximately 20 mi, 32 km, north of Victoria on Vancouver Island), and to the San Juan and Gulf islands, respectively. Ferries can also be taken from Port Angeles, Washington, to Victoria, British Columbia. In addition, ferries run regularly between islands in both Canada and Washington. Current ferry schedules are necessary for travel in this area.

Tidelands are considered public property in both Canada and the United States; access to the outcrops is available at many public beaches.
The Cenozoic section at Suntrana, Alaska
Authors: Wahrhaftig Clyde
Published: November 2007

The Cenozoic section at Suntrana in the Nenana coal field is located at Lat.63°52’N, Long.148°51’W, Healy D-4 Quadrangle, 3 to 3.5 mi (5 to 6 km) east of the Nenana River, on the north bank of Healy Creek and on Suntrana Creek, its 1.2-mi-long (2 km) tributary at this point (Figs. 1 and 2). It is approximately 6.7 mi (10.8 km) east, by automobile road, of mile 248.8 (km 400.4) on the George Parks Highway. Mile 248.8 is 7 mi (11.5 km) north on the highway from the entrance to Denali National Park. Suntrana Creek is narrow and shallow and is easily crossed dryshod most of the year. Its upper 1 mi (1.5 km) is usually dry. Vehicles should not be parked close to the crossing of Suntrana Creek, and one should not be in its canyon whenever storms are imminent, for during heavy rains masses of mud and water as much as 25 ft (8 m) deep have come raging down the creek.
Delta River area, Alaska Range, Alaska
Authors: Péwé Troy L.
Published: November 2007

The Alaska Range is a glacially sculptured, arcuate mountain wall extending west and southwest 600 mi (1,000 km) in central Alaska from the Canadian border to the Aleutian Range. It is extremely rugged and includes Mt. McKinley (20,443 ft; 6,195 m elevation), the highest mountain on the North American continent. The Delta River, 75 mi (125 km) long, originates on the south side of the range in the Tangle Lakes and flows northward through the range to the Tanana River. The Richard-son Highway (Fig, 1) crosses the range through the Delta River valley, which is 0.6 to 12 mi (1 to 20 km) wide and 60 mi (100 km) long. Because of the lack of villages, cities, and towns, references to geographical points in the valley have been referenced to mile posts on the Richardson Highway since the early part of this century. This practice will be continued in this report. Mile O on the highway is at Valdez, a town on the Gulf of Alaska and the terminus of the Trans-Alaska Pipeline System; the highway ends at mile Fairbanks 363.8.
Landslide and debris-flow deposits in the Thumb Member of the Miocene Horse Spring Formation on the east side of Frenchman Mountain, Nevada
Authors: Salyards Stephen L. , Shoemaker Eugene M.
Published: November 2007

From the south: From Henderson, Nevada, take Lake Mead Drive (Nevada 147). At 7.1 mi (11.4 km) east of U.S. 95, turn north onto Northshore Road and go 3.2 mi (5.1 km) to Lake Mead Boulevard. The site is 3.7 mi (6 km) north on Lake Mead Boulevard.

From the north: From North Las Vegas, take Lake Mead Boulevard (also Nevada 147) east from 1–15. At 11.4 mi (18.3 km) from 1–15 a paved road from the east (left) intersects Nevada 147. Continue on 147 for 1.8 mi (2.9 km) to the site.

The site is marked by the high-tension power line that crosses the road. Park along the side of the road or on the dirt roads that intersect the main road in this area.
Coastal and volcanic geology of the Hanauma Bay area, Oahu, Hawaii
Authors: Moberly Ralph , Walker George P. L.
Published: November 2007

The Hanauma Bay-Koko Fissure area occupies the southeastern tip of the island of Oahu, Hawaii (Fig. 1), and is shown on the Koko Head 71/2-minute Quadrangle. The Geologic Map of Oahu (1:62,500; Stearns, 1939) is out of print. A 1:500,000 colored geologic map of the state and generalized chart shows the Honolulu and Koolau volcanic groups-relative to other rock units (Bennison, 1974).

Access is easy by automobile. Buses of No. 1 route, marked “Lunalilo Home Road,” give frequent service from Honolulu to the Lunalilo Home Road point described below as mileage point zero. Buses of No. 58 route travel from Waikiki to that point. Traffic on the winding, narrow highway between stops 2 and 4 demands caution as does high surf on the seacliff. The area is within a park offering generally free access.
The Keystone and Red Spring thrust faults in the La Madre Mountain area, eastern Spring Mountains, Nevada
Authors: Axen Gary J.
Published: November 2007

The La Madre Mountain area lies about 9 mi (15 km) west of Las Vegas, Nevada (Fig. 1). Access is provided to sites 1 through 5 by side roads off of West Charleston Boulevard, and site 6 is reached from U.S. 95 northwest of town. The sites are meant to be visited in consecutive order, and the mileages given begin at the I-15 and West Charleston exit. Although the first fivesites are accessible by any vehicle, site 6 may necessitate a vehicle with a high center. Four-wheel drive is not necessary.

U.S. Geological Survey topographic maps for the area are the La Madre Mountain and Blue Diamond NE 7½-minute Quadrangles. Site 4 is on the easternmost edge of the Mountain Springs 15-minute Quadrangle.
Fault scarps formed during the earthquakes of October 2, 1915, Pleasant Valley, Nevada
Authors: Wallace Robert E.
Published: November 2007

Four fault scarps that formed during the earthquakes of October 2, 1915, are located in north-central Nevada, 150 mi (240 km) northeast of Reno, and 30 to 55 mi (48 to 88 km) south of Winnemucca (Fig. 1). A site along the largest of the four scarps, the Pearce scarp, at Golconda Canyon on the west flank of the Tobin Range (Sec. 5, T28N, R.39E, Mt. Tobin 15-minute Quadrangle) is easily reached by driving south about 45 mi (72 km) from Winnemucca along the Grass Valley-Pleasant Valley road, which is paved for about 7 mi (11.2 km) after which it is graded gravel. At the Golconda Canyon road, go east 1.5 mi (2.4 km) to the fault scarp at the range front. The Pearce scarp is also clearly visible from the Pleasant Valley road for about 15 mi (24 km) and excellent photo sites abound. Afternoon lighting emphasizes the scarp especially well. The Sou Hills scarp (3–6 ft) (l-2 m) high, can be seen in the distance to the south from near the junction of the Pleasant Valley-Dixie Valley roads. Additional map coverage is provided by the Cain Mountain and Fencemaker 15-minute and the China Mountain 71/2-minute Topographic Maps.
Lamoille Canyon nappe in the Ruby Mountains metamorphic core complex, Nevada
Authors: Howard Keith A.
Published: November 2007

Abstarct

The Ruby Mountains form a high and rugged range in northeastern Nevada. Lamoille Canyon in the Ruby Mountains is an easy half-hour drive by passenger car from the town of Elko (Fig. 1). From Elko, located on 1–80, take Nevada 227 southeast for 19 mi (30 km) to a sign marking a right turn onto the Lamoille Canyon road. This paved road leads south into the Ruby Mountains and ascends Lamoille Canyon for 10 mi (16 km) to an elevation of 8,730 ft (2,661 m). The site is best visited in summer, for the canyon is generally snowbound from November to May. The Lamoille Canyon road offers spectacular mountain scenery and a U.S. Forest Service campground. Geologic features are well exposed in roadside outcrops and in glaciated canyon walls 2,000 to 4,000 ft (600 to 1,200 m) high. To enhance your visit, bring a camera, a geologic road log (Snoke and Howard, 1984), a colored 1:125,000-scale geologic map (Howard and others, 1979), and the Lamoille, Nevada, 15-minute topographic quadrangle published by the U.S. Geological Survey.
Island Park, Idaho; Transition from rhyolites of the Yellowstone Plateau to basalts of the Snake River Plain
Authors: Christiansen Robert L. , Embree Glenn F.
Published: November 2007

Island Park, situated between the northeastern end of the Snake River Plain and the western margin of the Yellowstone Plateau, is traversed by U.S. 20-191 between Ashton, Idaho, and West Yellowstone, Montana (Fig. 1) and, in part, by the Mesa Falls Road (Idaho 47). All of the physiographic and geologic features described in this guide can be reached during the summer months by passenger car on those two paved highways or on short gravel roads that extend from them. During the winter, U.S. 20-191 remains open, but other winter travel is possible only by skis or skimobile. One quarry locality described later is privately owned but has generally been freely accessible.
A Neogene(?) gravity-slide block and associated slide phenomena in Swan Valley graben, Wyoming and Idaho
Authors: Moore David W. , Oriel Steven S. , Mabey Don R.
Published: November 2007

The gravity-slide block lies below the steep west flank of the Snake River Range near Alpine, Wyoming. Alpine is 37 mi (60 km) southwest of Jackson, Wyoming, via U.S. 89-26 and 73mi (117 km) east of Idaho Falls, Idaho, via U.S. 26. A Forest Service campground and several motels, restaurants, and stores are located at Alpine.

Rocks are well exposed at three stops on U.S. 26 north of Alpine along the east shore of Palisades Reservoir (Fig. 1). All stops are in the Targhee National Forest. No permission is required to visit them and all are accessible by passenger car when roads are dry. Stop 2 is reached by hiking 0.4 mi (0.7 km) overland and climbing 650 ft (200 m).

Stop 1 is in Long Springs Canyon (SW¼NW¼Sec.17,T.37N.,R.118W. on the Alpine Quadrangle map; Albee and Cullins, 1975). Drive 1.9 mi (3 km) north on U.S. 26 from the junction of U.S. 26 and 89 to a gravel road at the U.S. Forest Service sign“4-H Camp.” Turn east into Targhee National Forest and go 1.0 mi (1.6 km). Drive through the 4-H Camp and Idaho State University Geology Field Camp and across Long Springs Creek. An optional stop 1A is 0.2 mi (0.3 km) east and 0.2 mi (0.3 km) north.

Stop 2 is reached via an unimproved dirt road that is 1.3 mi (2.1 km) north of the 4-H Camp road intersection on U.S. 26. Drive east 0.5 mi (0.8 km) to the end of the dirt road. Walk upslope through the woods north-northeast to the base of the tan cliffs
Geology of the Craters of the Moon lava field, Idaho
Authors: Kuntz Mel A. , Champion Duane E. , Lefebvre Richard H.
Published: November 2007

The most convenient place to see the Craters of the Moon (COM) lava field is at Craters of the Moon National Monument, reached by U.S. 20-26 from either Arco or Carey, Idaho (Fig. 1). A 7-mi (11-km) loop road and several hiking trails provide accessto volcanic features within the Monument Fig. 2. The 20-mi long (32-km) Wilderness Trail is the longest of the trails and requires a permit for overnight trips; there is no potable water available along this trail. The east, south, and west edges of the COM lava field can be reached by four-wheel-drive vehicles on unimproved roads that are shown on U.S. Geological Survey 7½-minute quadrangle maps of the area. The geologie map of the Inferno Cone Quadrangle (Kuntz and others, 1986c) depicts the volcanic features that are most accessible to visitors to the monument. Please note that hammers may not be used and samples may not be taken in the monument.