Many amphibians breed in water but live most of their lives in terrestrial habitats. Little is known, however, about the spatial distribution of these habitats or of the distances and directions amphibians move to reach breeding sites. The amphibian community at a small, temporary pond in northcentral Florida was monitored for 5 years. Based on captures and recaptures of more than 2500 striped newts (Notophthalmus perstriatus) and 5700 eastern narrow-mouthed toads (Gastrophryne carolinensis), we tabulated the angles of orientation that these amphibians entered and exited the pond basin. Our results showed that movements of these species between the pond and terrestrial habitats were nonrandom in orientation, but that narrow corridors did not appear to be used. Differences between the species likely reflect differences in habitat preferences, whereas intraspecific differences among years and between the sexes likely reflect variation among individuals. For terrestrial buffer zones to be effective at conserving pond-breeding amphibian communities, they need both a distance and a directional component. The determination of a directional component may be obscured if studies are carried out over a short time span. Conservation efforts for wetland-breeding amphibians that concentrate solely on the wetland likely will fail without consideration of the adjacent terrestrial habitat.
","language":"English","publisher":"Wiley","doi":"10.1111/j.1523-1739.1998.97183.x","issn":"08888892","usgsCitation":"Dodd, C., and Cade, B., 1998, Movement patterns and the conservation of amphibians breeding in small, temporary wetlands: Conservation Biology, v. 12, no. 2, p. 331-339, https://doi.org/10.1111/j.1523-1739.1998.97183.x.","productDescription":"9 p.","startPage":"331","endPage":"339","costCenters":[],"links":[{"id":229937,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida","county":"Putnam County","otherGeospatial":"Breezeway Pond","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -81.95662307562839,\n 29.696250615108752\n ],\n [\n -81.95662307562839,\n 29.693652539858803\n ],\n [\n -81.95341602191513,\n 29.693652539858803\n ],\n [\n -81.95341602191513,\n 29.696250615108752\n ],\n [\n -81.95662307562839,\n 29.696250615108752\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"12","issue":"2","noUsgsAuthors":false,"publicationDate":"2008-07-07","publicationStatus":"PW","scienceBaseUri":"505a5f2ae4b0c8380cd70de6","contributors":{"authors":[{"text":"Dodd, C.K. Jr.","contributorId":86286,"corporation":false,"usgs":true,"family":"Dodd","given":"C.K.","suffix":"Jr.","affiliations":[],"preferred":false,"id":388770,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cade, B.S.","contributorId":47315,"corporation":false,"usgs":true,"family":"Cade","given":"B.S.","affiliations":[],"preferred":false,"id":388769,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70021345,"text":"70021345 - 1998 - Palynology of latest Neogene (Middle Miocene to late Pliocene) strata in the Delmarva Peninsula of Maryland and Virginia","interactions":[],"lastModifiedDate":"2012-03-12T17:19:50","indexId":"70021345","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2897,"text":"Northeastern Geology and Environmental Sciences","active":true,"publicationSubtype":{"id":10}},"title":"Palynology of latest Neogene (Middle Miocene to late Pliocene) strata in the Delmarva Peninsula of Maryland and Virginia","docAbstract":"Palynology of Miocene and Pliocene formations in the Delmarva Peninsula of Maryland and Virginia reveals a significant representation of exotic pollen interspersed in pollen assemblages that are otherwise comparable to those from the modern vegetation of the Mid-Alantic coastal plain region. The late Tertiary arboreal pollen (AP) assemblages are dominated by oak, hickory, pine, birch and alder with minor amounts of mid- and southern coastal tree taxa, as well as minor spruce and hemlock and a trace of fir. Nonarboreal pollen (NAP) include grass, sedge, composite and aquatic taxa. Exotic pollen in these assemblages represent plants now foreign to this region. They may be placed in three categories. First, there are extinct forms, such as Labrapollis, Plicatopollis, and Multiporopollenites, that can be traced from the Cretaceous or Early Tertiary into the Late Tertiary. The second group includes forms, such as Podocarpus, Engelhardtia, Pterocarya, Ephedra, Eucommia, Ulmus-Zelkova, Glyptostrobus, Palmae, and Cyathea, that are not found in this region today and not found in early Pleistocene sediments in the eastern United States. Many of these taxa are subtropical or greatly restricted in geographic range. A third group of exotics, mainly Cyrilla, Planera, Gordonia, Jussiaea, and Sapotacaea, including Minusops, are generally found south of the study area or have their northern limit here at this time. The lack of the extinct or distant exotics in early to mid-Pleistocene sediments in the mid-Atlantic coastal plain and the last appearance of Pterocarya, as the last exotic taxon in the early Pleistocene of western Europe, support the stratigraphic assignment of the Pliocene units. The number of exotic taxa diminish markedly between the Miocene pollen assemblages and those of the Late Pliocene. Climatic fluctuations characterize the Late Tertiary environments. The Miocene, for example, incorporates a warming trend between the upper, middle Miocene and the Manokin beds and the late Miocene of the Pokomoke beds. The late Miocene was probably somewhat warner than the present climate in the Delmarva region. This trend is based on the presence of colder climate indicators, mainly spruce and hemlock, in the Manokin pollen record. The two distinct pollen assemblages constitute two pollen zones. Similarly, the Pliocene pollen record also shows a warming trend. The pollen zone of the Yorktown Formation of the early Pliocene age contains the colder climate indicators spruce and hemlock. The Beaverdam and Walston formation of late Pliocene age contain pollen assemblages that reflect climatic conditions warmer than the present time.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Northeastern Geology and Environmental Sciences","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","issn":"01941453","usgsCitation":"Sirkin, L., and Owens, J.P., 1998, Palynology of latest Neogene (Middle Miocene to late Pliocene) strata in the Delmarva Peninsula of Maryland and Virginia: Northeastern Geology and Environmental Sciences, v. 20, no. 2, p. 117-132.","startPage":"117","endPage":"132","numberOfPages":"16","costCenters":[],"links":[{"id":230267,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"20","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a74a1e4b0c8380cd77739","contributors":{"authors":[{"text":"Sirkin, L.","contributorId":63954,"corporation":false,"usgs":true,"family":"Sirkin","given":"L.","email":"","affiliations":[],"preferred":false,"id":389543,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Owens, J. P.","contributorId":50946,"corporation":false,"usgs":true,"family":"Owens","given":"J.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":389542,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1014868,"text":"1014868 - 1998 - Biochemical and conjugation studies of romet-resistant strains of Aeromonas salmonicida from salmonid rearing facilities in the eastern United States","interactions":[],"lastModifiedDate":"2024-03-01T00:56:53.624526","indexId":"1014868","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2177,"text":"Journal of Aquatic Animal Health","active":true,"publicationSubtype":{"id":10}},"title":"Biochemical and conjugation studies of romet-resistant strains of Aeromonas salmonicida from salmonid rearing facilities in the eastern United States","docAbstract":"Strains of Aeromonas salmonicida (n = 585) were collected from covertly infected and diseased salmonid hosts from 12 hatcheries in the eastern United States. Strains and sites were selected because of their potential for harboring antimicrobial resistance, in particular, to Romet™. Resistance to Romet was displayed by 315 strains (53.8%), which were isolated from all six host species sampled at 10 of 12 sites. Thirty of the resistant strains (9.5%) from five sites had no zone of inhibition, whereas the other strains had either confluent growth or resistant colonies within a zone of inhibition. Fifty-one resistant strains, representing each of the three resistance phenotypes, were selected for biochemical and antimicrobial comparisons with Romet-sensitive strains. All were confirmed to be A. salmonicida, and no characteristic biochemical phenotypes were found to be associated with resistance to Romet. Differential resistances between resistant and sensitive strains were detected to the antimicrobials oxytetracycline, tetracycline, sulfadiazine, sulfamethizole, trimethoprim, and SXT, a potentiated sulfonamide composed of trimethoprim and sulfamethoxazole. Plasmid DNA isolation and agarose gel electrophoresis were done for 25 Romet-resistant strains, and R-plasmids, not present in sensitive strains, were detected in 23 of these. Two different sizes of R-plasmids were detected, one about 55 kilobase pairs long and another about 50 kilobase pairs. Two strains isolated from New York brook trout Salvelinus fontinalis had reduced confluent growth within a zone of inhibition but contained no large plasmids. This may indicate chromosomally mediated resistance. Conjugational mating studies evaluated transfer of the R-plasmid DNA using eight Escherichia coli recipients. Successful R-plasmid transfer was accomplished with two donor strains (MI1 and MI2 from New Hampshire brook trout). Our results, in addition to those of other workers, illustrate the widespread resistance in A. salmonicida to approved antimicrobials and the capacity of this bacterium to become resistant in the fish culture environment.
This study had two primary objectives: to conduct roost surveys C. townsendii in two parts of California where distributional information was most limited or lacking, and to obtain information on roosting and foraging ecology in two distinctly different habitats. This project was urgently needed because 1) recent California Department of Fish and Game surveys (conducted in 1987-1991) documented significant population declines in most surveyed areas, 2) distribution was still unknown in areas with suitable roosting habitat, and 30 the impact of various land management practices (e.g. prescribed fire, timber, harvest, agriculture, and grazing) on foraging behavior was unknown.
\nA total of 95 abandoned mines, 18 caves, 11 man-made water tunnels, and 7 buildings were surveys for bats. Twenty-pne structures (twelve caves and nine mines) showed significant use by C. townsendii. Eleven are located in the western Sierra Nevada foothills, and ten in the Trinity Mountain area, Six maternity colonies, ranging in size from 48 to about 250 adult females, were identifies. Three were in caves, and three were in mines.
\nDistribution for this species is somewhat patchy, and appears to be limited by the availability of roosting habitat. Historic and recent records would suggest that populations are concentrated in areas with abundant caves (especially the large lava flows in the northeastern portion of the state and karstic regions in the Sierra Nevada and Trinity Alps) or extensive abandoned mine working (particularly in the desert regions to the east and southeast of the Sierra Nevada).
\nRadiotracking studies were conducted in two different habitats: 1) coastal forest (California bay, Douglas fir, and redwood) and grazed grassland at Pt. Reyes National Seashore, and 2) a mixture of scrub (with juniper and mountain mahogany) and ponderosa pine forest at Lava Beds National Monument. At Point Reyes they study colony resided in an abandoned ranch house, and at Lava Beds in a lava tube. In both settings the animals showed considerable loyalty to their roost sites even though the study was conducted after the nursery season had ended; females traveled greater distances than males to forage; and all the animals foraged in close association with vegetation -- in the vegetated gullies and redwood forest at Pt. Reyes, and in the vegetated lava trenches, near juniper or mountain mahogany, and with the stands of ponderosa pine at Lava Beds.
\nGenetic variation was preliminarily examined for three populations using mitochondrial DNA and microsatellites -- two populations within the zone of intergradation between the two subspecies, C. t. townsendii and C. t. pallescens, and one population from the range of C. t. pallescens. These three populations were sufficiently distinct genetically to suggest that these techniques would be appropriated for addressing a wide range of questions for this species, including population differentiation, gene flow and mating systems.
\nMost maternity populations appear to be declining in numbers, and many historic colonies no longer exist. The primary threat to this species appears to be human disturbance at roost sites, particularly recreational caving, renewed mining in old mining districts, and reclamation of abandoned mines for hazard abatement.
","language":"English","publisher":"California Department of Fish and Wildlife","publisherLocation":"Sacremento, CA","collaboration":"Prepared for: Department of the Interiors U.S. Geological Survey Biological Resources Division Species at Risk Program Fiscal Year 1998","usgsCitation":"Pierson, E.D., and Fellers, G.M., 1998, Distribution and ecology of the big-eared bat, Corynorhinus (=Plecotus) townsendii in Californa, i, 90 p.","productDescription":"i, 90 p.","numberOfPages":"95","costCenters":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"links":[{"id":198979,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -125.0,32.0 ], [ -125.0,43.0 ], [ -115.0,43.0 ], [ -115.0,32.0 ], [ -125.0,32.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a81e4b07f02db64a181","contributors":{"authors":[{"text":"Pierson, Elizabeth D.","contributorId":48139,"corporation":false,"usgs":true,"family":"Pierson","given":"Elizabeth","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":326276,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fellers, Gary M. 0000-0003-4092-0285 gary_fellers@usgs.gov","orcid":"https://orcid.org/0000-0003-4092-0285","contributorId":3150,"corporation":false,"usgs":true,"family":"Fellers","given":"Gary","email":"gary_fellers@usgs.gov","middleInitial":"M.","affiliations":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"preferred":true,"id":326275,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":87325,"text":"87325 - 1998 - Translocated sea otter populations off the coasts of Oregon and Washington","interactions":[{"subject":{"id":87325,"text":"87325 - 1998 - Translocated sea otter populations off the coasts of Oregon and Washington","indexId":"87325","publicationYear":"1998","noYear":false,"title":"Translocated sea otter populations off the coasts of Oregon and Washington"},"predicate":"IS_PART_OF","object":{"id":70103848,"text":"70103848 - 1998 - Status and trends of the nation's biological resources","indexId":"70103848","publicationYear":"1998","noYear":false,"title":"Status and trends of the nation's biological resources"},"id":1}],"isPartOf":{"id":70103848,"text":"70103848 - 1998 - Status and trends of the nation's biological resources","indexId":"70103848","publicationYear":"1998","noYear":false,"title":"Status and trends of the nation's biological resources"},"lastModifiedDate":"2019-08-09T16:02:26","indexId":"87325","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Translocated sea otter populations off the coasts of Oregon and Washington","docAbstract":"The historical distribution of sea otters extended from the northern islands of Japan north and east across the Aleutian chain to the mainland of North America then south along the west coast to central Baja California, Mexico (Riedman and Estes 1990). By the beginning of the twentieth century, after 150 years of being intensively hunted for their valuable fur, sea otters had been extirpated from most of their range (Kenyon 1969). In 1911 sea otters were protected by the passage of the International Fur Seal Treaty. Unfortunately, only 13 remnant populations survived the fur-hunting period, and two of those, British Columbia and Mexico, would also ultimately disappear, leaving only a small group of sea otters south of Alaska, along the rugged Big Sur coast of California (Kenyon 1969).
The earliest attempts to reestablish sea otters to unoccupied habitat were begun in the early 1950’s by R. D. (Sea Otter) Jones, then manager of the Aleutian National Wildlife Refuge (Kenyon 1969). These early efforts were experimental, and all failed to establish populations. However, the knowledge gained from Jones’s efforts and the seminal work of Kenyon (1969) and others during the 1950’s and early 1960’s ultimately led to the successful efforts to come.
During the mid-1960’s the Alaska Department of Fish and Game began translocating sea otters to sites where the species had occurred before the fur-trade period. The first translocations were restricted to Alaska, but beginning in 1969 and continuing through 1972, the effort expanded beyond Alaska. During this period, 241 sea otters were translocated to sites in British Columbia, Washington, and Oregon (Jameson et al. 1982). The work was done cooperatively between state and provincial conservation agencies, with much of the financial support for the Oregon and Washington efforts coming from the Atomic Energy Commission (now ERDA). Followup studies of the Oregon population began in 1971 and continued through 1975. After 1975, surveys in Oregon occurred infrequently. In Washington no follow-up surveys were conducted until 1977, although the population has been monitored closely since then (Jameson et al. 1982, 1986; Jeffries and Jameson 1995).
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Status and trends of the nation's biological resources","largerWorkSubtype":{"id":9,"text":"Other Report"},"language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","isbn":"016053285X","usgsCitation":"Jameson, R.J., 1998, Translocated sea otter populations off the coasts of Oregon and Washington, chap. of Status and trends of the nation's biological resources, p. 684-686.","productDescription":"3 p.","startPage":"684","endPage":"686","costCenters":[{"id":651,"text":"Western Ecological Research Center","active":true,"usgs":true}],"links":[{"id":128414,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Oregon, Washington","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db626e1e","contributors":{"editors":[{"text":"Mac, Michael J.","contributorId":16772,"corporation":false,"usgs":true,"family":"Mac","given":"Michael","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":504988,"contributorType":{"id":2,"text":"Editors"},"rank":1},{"text":"Opler, Paul A.","contributorId":86690,"corporation":false,"usgs":true,"family":"Opler","given":"Paul","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":504989,"contributorType":{"id":2,"text":"Editors"},"rank":2},{"text":"Puckett Haecker, Catherine E.","contributorId":45630,"corporation":false,"usgs":true,"family":"Puckett Haecker","given":"Catherine","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":504990,"contributorType":{"id":2,"text":"Editors"},"rank":3},{"text":"Doran, Peter D.","contributorId":17533,"corporation":false,"usgs":true,"family":"Doran","given":"Peter","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":504991,"contributorType":{"id":2,"text":"Editors"},"rank":4}],"authors":[{"text":"Jameson, Ronald J.","contributorId":17938,"corporation":false,"usgs":true,"family":"Jameson","given":"Ronald","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":297669,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70021039,"text":"70021039 - 1998 - 40Ar/39Ar age of the Manson impact structure, Iowa, and correlative impact ejecta in the Crow Creek member of the Pierre Shale (Upper Cretaceous), South Dakota and Nebraska","interactions":[],"lastModifiedDate":"2023-12-20T12:24:51.240061","indexId":"70021039","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"40Ar/39Ar age of the Manson impact structure, Iowa, and correlative impact ejecta in the Crow Creek member of the Pierre Shale (Upper Cretaceous), South Dakota and Nebraska","docAbstract":"A set of 34 laser total-fusion 40Ar/39Ar analyses of sanidine from a melt layer in crater-fill deposits of the Manson impact structure in Iowa has a weighted-mean age of 74.1 ± 0.1 Ma. This age is about 9.0 m.y. older than 40Ar/39Ar ages of shocked microcline from the Manson impact structure reported previously by others. The 74.1 Ma age of the sanidine, which is a melt product of Precambrian microcline clasts, indicates that the Manson impact structure played no part in the Cretaceous-Tertiary (K-T) mass extinction at 64.5 Ma. Moreover, incremental-heating 40Ar/39Ar ages of the sanidine show that it is essentially free of excess 40Ar and has not been influenced by postcrystallization heating or alteration. An age spectrum of the matrix of the melt layer shows effects of 39Ar recoil, including older ages in the low-temperature increments and younger ages in the high-temperature increments. At 17 places in eastern South Dakota and Nebraska, shocked quartz and feldspar grains are concentrated in the lower part of the Crow Creek Member of the Pierre Shale (Upper Cretaceous). The grains are largest (3.2 mm) in southeastern South Dakota and decrease in size (0.45 mm) to the northwest, consistent with the idea that the Manson impact structure was their source. The ubiquitous presence of shocked grains concentrated in a thin calcarenite at the base of the Crow Creek Member suggests it is an event bed recording an instant of geologic time. Ammonites below and above the Crow Creek Member limit its age to the zone of Didymoceras nebrascense of earliest late Campanian age. Plagioclase from a bentonite bed in this zone in Colorado has a 40Ar/39Ar age of 74.1 ± 0.1 Ma commensurate with our sanidine age of 74.1 Ma for the Manson impact structure. 40Ar/39Ar ages of bentonite beds below and above the Crow Creek are consistent with our 74.1 ± 0.1 Ma age for the Manson impact structure and limit its age to the interval ±74.5 0.1 to 73.8 ± 0.1 Ma. Recently, two origins for the Crow Creek have been proposed—eastward transgression of the Late Cretaceous sea and a Manson impact-triggered tsunami. We conclude that most data are in accord with an impact origin for the Crow Creek Member and are at odds with the marine transgression hypothesis.
In light of suggestions that the Cascadia subduction margin may pose a significant seismic hazard for the highly populated Pacific Northwest region of the United States, the U.S. Geological Survey (USGS), the Research Center for Marine Geosciences (GEOMAR), and university collaborators collected and interpreted a 530-km-long wide-angle onshore-offshore seismic transect across the subduction zone and volcanic arc to study the major structures that contribute to seismogenic deformation. We observed (1) an increase in the dip of the Juan de Fuca slab from 2°–7° to 12° where it encounters a 20-km-thick block of the Siletz terrane or other accreted oceanic crust, (2) a distinct transition from Siletz crust into Cascade arc crust that coincides with the Mount St. Helens seismic zone, supporting the idea that the mafic Siletz block focuses seismic deformation at its edges, and (3) a crustal root (35–45 km deep) beneath the Cascade Range, with thinner crust (30–35 km) east of the volcanic arc beneath the Columbia Plateau flood basalt province. From the measured crustal structure and subduction geometry, we identify two zones that may concentrate future seismic activity: (1) a broad (because of the shallow dip), possibly locked part of the interplate contact that extends from ∼25 km depth beneath the coastline to perhaps as far west as the deformation front ∼120 km offshore and (2) a crustal zone at the eastern boundary between the Siletz terrane and the Cascade Range.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0091-7613(1998)026<0199:ANVITC>2.3.CO;2","issn":"00917613","usgsCitation":"Parsons, T., Trehu, A., Luetgert, J., Miller, K., Kilbride, F., Wells, R., Fisher, M.A., Flueh, E., ten Brink, U., and Christensen, N., 1998, A new view into the Cascadia subduction zone and volcanic arc: Implications for earthquake hazards along the Washington margin: Geology, v. 26, no. 3, p. 199-202, https://doi.org/10.1130/0091-7613(1998)026<0199:ANVITC>2.3.CO;2.","productDescription":"4 p.","startPage":"199","endPage":"202","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":230135,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Cascadia","volume":"26","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e4bae4b0c8380cd468a4","contributors":{"authors":[{"text":"Parsons, T.","contributorId":48288,"corporation":false,"usgs":true,"family":"Parsons","given":"T.","email":"","affiliations":[],"preferred":false,"id":388665,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trehu, A.M.","contributorId":90754,"corporation":false,"usgs":true,"family":"Trehu","given":"A.M.","email":"","affiliations":[],"preferred":false,"id":388672,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Luetgert, J.H.","contributorId":69993,"corporation":false,"usgs":true,"family":"Luetgert","given":"J.H.","email":"","affiliations":[],"preferred":false,"id":388670,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Miller, K.","contributorId":104434,"corporation":false,"usgs":true,"family":"Miller","given":"K.","affiliations":[],"preferred":false,"id":388673,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Kilbride, F.","contributorId":56407,"corporation":false,"usgs":true,"family":"Kilbride","given":"F.","email":"","affiliations":[],"preferred":false,"id":388667,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Wells, R.E. 0000-0002-7796-0160","orcid":"https://orcid.org/0000-0002-7796-0160","contributorId":67537,"corporation":false,"usgs":true,"family":"Wells","given":"R.E.","affiliations":[],"preferred":false,"id":388668,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Fisher, M. A.","contributorId":69972,"corporation":false,"usgs":true,"family":"Fisher","given":"M.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":388669,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Flueh, E.","contributorId":55591,"corporation":false,"usgs":true,"family":"Flueh","given":"E.","email":"","affiliations":[],"preferred":false,"id":388666,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"ten Brink, Uri S. 0000-0001-6858-3001 utenbrink@usgs.gov","orcid":"https://orcid.org/0000-0001-6858-3001","contributorId":127560,"corporation":false,"usgs":true,"family":"ten Brink","given":"Uri S.","email":"utenbrink@usgs.gov","affiliations":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true},{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":388671,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Christensen, N.I.","contributorId":28016,"corporation":false,"usgs":true,"family":"Christensen","given":"N.I.","email":"","affiliations":[],"preferred":false,"id":388664,"contributorType":{"id":1,"text":"Authors"},"rank":10}]}} ,{"id":22061,"text":"ofr98360 - 1998 - Preliminary volcano-hazard assessment for Akutan Volcano, east-central Aleutian Islands, Alaska","interactions":[],"lastModifiedDate":"2022-12-21T20:26:43.652431","indexId":"ofr98360","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"98-360","title":"Preliminary volcano-hazard assessment for Akutan Volcano, east-central Aleutian Islands, Alaska","docAbstract":"Akutan Volcano is a 1100-meter-high stratovolcano on Akutan Island in the east-central Aleutian Islands of southwestern Alaska. The volcano is located about 1238 kilometers southwest of Anchorage and about 56 kilometers east of Dutch Harbor/Unalaska. Eruptive activity has occurred at least 27 times since historical observations were recorded beginning in the late 1700's. Recent eruptions produced only small amounts of fine volcanic ash that fell primarily on the upper flanks of the volcano. Small amounts of ash fell on the Akutan Harbor area during eruptions in 1911, 1948, 1987, and 1989. Plumes of volcanic ash are the primary hazard associated with eruptions of Akutan Volcano and are a major hazard to all aircraft using the airfield at Dutch Harbor or approaching Akutan Island. Eruptions similar to historical Akutan eruptions should be anticipated in the future. Although unlikely, eruptions larger than those of historical time could generate significant amounts of volcanic ash, fallout, pyroclastic flows, and lahars that would be hazardous to life and property on all sectors of the volcano and other parts of the island, but especially in the major valleys that head on the volcano flanks. During a large eruption an ash cloud could be produced that may be hazardous to aircraft using the airfield at Cold Bay and the airspace downwind from the volcano. In the event of a large eruption, volcanic ash fallout could be relatively thick over parts of Akutan Island and volcanic bombs could strike areas more than 10 kilometers from the volcano.
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The sulfonic and oxanilic metabolites were present in almost 75% of the groundwater samples and were generally present from 3 to 45 times more frequently than their parent compounds. In groundwater, the median value of the summed concentrations of acetochlor, alachlor, and metolachlor was less than 0.05 μg/L, and the median value of the summed concentrations of the six metabolites was 1.2 μg/L. All surface water samples contained at least one detectable metabolite compound. Individual metabolites were detected from 2 to over 100 times more frequently than the parent compounds. In surface water, the median value of the summed concentrations of the three parent compounds was 0.13 μg/L, and the median value of the summed concentrations of the six metabolites was 6.4 μg/L. These data demonstrate the importance of analyzing both parent compounds and metabolites to more fully understand the environmental fate and transport of herbicides in the hydrologic system.
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D.","contributorId":24107,"corporation":false,"usgs":true,"family":"Barcelo","given":"D.","affiliations":[],"preferred":false,"id":385930,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70020513,"text":"70020513 - 1998 - Geohistory and thermal maturation in the Cherokee Basin (Mid-Continent, U.S.A.): results from modeling","interactions":[],"lastModifiedDate":"2012-03-12T17:20:18","indexId":"70020513","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Geohistory and thermal maturation in the Cherokee Basin (Mid-Continent, U.S.A.): results from modeling","docAbstract":"The Cherokee basin in southeastern Kansas contains a stratigraphic section consisting mostly of Permian-Pennsylvanian alternating clastics and thin carbonates overlying carbonates of Mississippian and Cambrian-Ordovician age on a Precambrian crytalline basement. Based on a conceptual model of events of deposition, nondeposition, and erosion, a burial history model for (1) noncompaction, and a series of models for (2) compaction are computed for a borehole location in the south-central part of the basin. The models are copled with the calculation of nonsteady-state geothermal conditions. Maximum temperatures during basin evolution of about 70??C at the base of the organic-rich Pennsylvanian are predicted by our models, assuming pure heat conduction and a heat flow from the basement of 60 m W/m2. The maturation of organic matter as indicated by three different vitrinite reflectance (Ro) models is on the order og 0.3-0.5% Ro for Pennsylvanian rocks and 0.6% Ro for the Devonian-Mississippian Cattanooga Shale. Vitrinite reflectance was measured on subsurface smaples from three wells. The measured values correlate in the upper part of the sequence with modeled data, but diverge slightly in the Lower Pennsylvanian and Cattanooga Shale. The differences in maturation may be a result of differing local geological conditions within the basin. The relatively high Ro-depth gradients observed in one borehole may be explained by conditions in the Teeter oil field, which is a typical plains-type anticline that has been affected by fluid flow through vertical faults. Higher Ro values correlate positively with the grade of sulfidfe mineralization in the sediment, which may be a hint of fluid impact. The high Ro values relative to the shallow depth of the Mississippian and the Chattanooga Shale in the Brown well are on the order of Ro values modeled for the same stratigraphic units at present-day greater depths and may reflect uplift of the Ozark dome, located further east, affecting the eastern side of the Cherokee Basin.Based on a concept model of deposition, nondeposition and erosion, a burial history model for noncompaction, and a series of models for compaction are developed for a borehole location in a south-central part of the Cherokee basin in southeastern Kansas. Coupled with the calculation of nonsteady state-state geothermal conditions, the models predict maximum temperatures during evolution of about 70 ??C at the base of the organic-rich Pennsylvanian. A difference in organic matter maturation in the Pennsylvanian and the Chattanooga shale exhibited by vitrinite reflectance models indicate probably differing local geological conditions within the basin.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"American Association of Petroleum Geologists Bulletin","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"AAPG","publisherLocation":"Tulsa, OK, United States","issn":"01491423","usgsCitation":"Forster, A., Merriam, D.F., and Hoth, P., 1998, Geohistory and thermal maturation in the Cherokee Basin (Mid-Continent, U.S.A.): results from modeling: American Association of Petroleum Geologists Bulletin, v. 82, no. 9, p. 1673-1693.","startPage":"1673","endPage":"1693","numberOfPages":"21","costCenters":[],"links":[{"id":231186,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"82","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a1799e4b0c8380cd55565","contributors":{"authors":[{"text":"Forster, A.","contributorId":14580,"corporation":false,"usgs":true,"family":"Forster","given":"A.","email":"","affiliations":[],"preferred":false,"id":386501,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Merriam, D. F.","contributorId":63175,"corporation":false,"usgs":true,"family":"Merriam","given":"D.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":386503,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hoth, P.","contributorId":37215,"corporation":false,"usgs":true,"family":"Hoth","given":"P.","email":"","affiliations":[],"preferred":false,"id":386502,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70020618,"text":"70020618 - 1998 - Structural and kinematic evolution of the Yukon-Tanana upland tectonites, east-central Alaska: A record of late Paleozoic to Mesozoic crustal assembly","interactions":[],"lastModifiedDate":"2019-12-17T14:00:57","indexId":"70020618","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Structural and kinematic evolution of the Yukon-Tanana upland tectonites, east-central Alaska: A record of late Paleozoic to Mesozoic crustal assembly","docAbstract":"The Yukon-Tanana terrane, the largest tectonostratigraphic terrane in the northern North American Cordillera, is polygenetic and not a single terrane. Lineated and foliated (L-S) tectonites, which characterize the Yukon-Tanana terrane, record multiple deformations and formed at different times. We document the polyphase history recorded by L-S tectonites within the Yukon-Tanana upland, east-central Alaska. These upland tectonites compose a heterogeneous assemblage of deformed igneous and metamorphic rocks that form the Alaskan part of what has been called the Yukon-Tanana composite terrane. We build on previous kinematic data and establish the three-dimensional architecture of the upland tectonites through kinematic and structural analysis of more than 250 oriented samples, including quartz c-axis fabric analysis of 39 samples. Through this study we distinguish allochthonous tectonites from parautochthonous tectonites within the Yukon-Tanana upland. The upland tectonites define a regionally coherent stacking order: from bottom to top, they are lower plate North American parautochthonous attenuated continental margin; continentally derived marginal-basin strata; and upper plate ocean-basin and island-arc rocks, including some continental basement rocks. We delineate three major deformation events in time, space, and structural level across the upland from the United States-Canada border to Fairbanks, Alaska: (1) pre-Early Jurassic (>212 Ma) northeast-directed, apparent margin-normal contraction that affected oceanic rocks; (2) late Early to early Middle Jurassic (>188-185 Ma) northwest-directed, apparent margin-parallel contraction and imbrication that resulted in juxtaposition of the allochthonous tectonites with parautochthonous continental rocks; and (3) Early Cretaceous (135-110 Ma) southeast-directed crustal extension that resulted in exposure of the structurally deepest, parautochthonous continental rocks. The oldest event represents deformation within a west-dipping (present coordinates) Permian-Triassic subduction zone. The second event records Early to Middle Jurassic collision of the arc and subduction complex with North American crust, and the third event reflects mid-Cretaceous southeast-directed crustal extension. Events one and two can be recognized and correlated through southern Yukon, even though this region was affected by mid-Cretaceous dextral shear along steep northwest-striking faults. Our data support a model of crustal assembly originally proposed by D. Tempelman-Kluit in which previously deformed allochthonous rocks were thrust over parautochthonous rocks of the attenuated North American margin in Middle Jurassic time. Approximately 50 m.y. after tectonic accretion, east-central Alaska was dissected by crustal extension, exposing overthrust parautochthonous strata.","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1998)110<0211:SAKEOT>2.3.CO;2","issn":"00167606","usgsCitation":"Hansen, V.L., and Dusel-Bacon, C., 1998, Structural and kinematic evolution of the Yukon-Tanana upland tectonites, east-central Alaska: A record of late Paleozoic to Mesozoic crustal assembly: Geological Society of America Bulletin, v. 110, no. 2, p. 211-230, https://doi.org/10.1130/0016-7606(1998)110<0211:SAKEOT>2.3.CO;2.","productDescription":"20 p.","startPage":"211","endPage":"230","numberOfPages":"20","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":231149,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Yukon-Tanana Upland","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -154.248046875,\n 60.88770004207789\n ],\n [\n -141.15234374999997,\n 60.88770004207789\n ],\n [\n -141.15234374999997,\n 66.93006025862448\n ],\n [\n -154.248046875,\n 66.93006025862448\n ],\n [\n -154.248046875,\n 60.88770004207789\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"110","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b9bc7e4b08c986b31d0ae","contributors":{"authors":[{"text":"Hansen, V. L.","contributorId":82400,"corporation":false,"usgs":true,"family":"Hansen","given":"V.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":386881,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dusel-Bacon, Cynthia 0000-0001-8481-739X cdusel@usgs.gov","orcid":"https://orcid.org/0000-0001-8481-739X","contributorId":2797,"corporation":false,"usgs":true,"family":"Dusel-Bacon","given":"Cynthia","email":"cdusel@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":777781,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":7000020,"text":"7000020 - 1998 - Glimpses of the Ice Age from I-81: Lee Ranger District","interactions":[],"lastModifiedDate":"2015-06-04T08:46:50","indexId":"7000020","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":363,"text":"General Interest Publication","active":false,"publicationSubtype":{"id":6}},"subseriesTitle":"Geologic wonders of the George Washington and Jefferson National Forests, No. 1","title":"Glimpses of the Ice Age from I-81: Lee Ranger District","docAbstract":"Travelers on Interstate Highway 81 can see remnants of the Ice Age on the mountains between Strasburg and Harrisonburg, Virginia. Scattered along the miles of green, forested mountains are many gray patches without any forests. These treeless patches, or openings, in the steep mountain forests are block fields - geologic features that owe their origin to the Ice Age.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/7000020","usgsCitation":"Water Resources Division, U.S. Geological Survey, and U.S. Forest Service, 1998, Glimpses of the Ice Age from I-81: Lee Ranger District: General Interest Publication, Pamphlet: 4 p., https://doi.org/10.3133/7000020.","productDescription":"Pamphlet: 4 p.","numberOfPages":"4","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":300867,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/7000020.jpg"},{"id":300859,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gip/i81/i81.pdf","text":"report","size":"172 K","linkFileType":{"id":1,"text":"pdf"},"description":"report"},{"id":18592,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/gip/i81/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Virginia","otherGeospatial":"Passage Creek, Woodstock Tower","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.30986022949217,\n 38.94125285438687\n ],\n [\n -78.30986022949217,\n 38.966382907015735\n ],\n [\n -78.28707218170166,\n 38.966382907015735\n ],\n [\n -78.28707218170166,\n 38.94125285438687\n ],\n [\n -78.30986022949217,\n 38.94125285438687\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.5059404373169,\n 38.87189044926606\n ],\n [\n -78.5059404373169,\n 38.88224734948839\n ],\n [\n -78.46392631530762,\n 38.88224734948839\n ],\n [\n -78.46392631530762,\n 38.87189044926606\n ],\n [\n -78.5059404373169,\n 38.87189044926606\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abee4b07f02db674dfa","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":547770,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"U.S. Forest Service","contributorId":128067,"corporation":true,"usgs":false,"organization":"U.S. Forest Service","id":547771,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70020611,"text":"70020611 - 1998 - Stress transferred by the 1995 Mw = 6.9 Kobe, Japan, shock: Effect on aftershocks and future earthquake probabilities","interactions":[],"lastModifiedDate":"2024-07-19T14:13:03.842943","indexId":"70020611","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2314,"text":"Journal of Geophysical Research B: Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Stress transferred by the 1995 Mw = 6.9 Kobe, Japan, shock: Effect on aftershocks and future earthquake probabilities","docAbstract":"The Kobe earthquake struck at the edge of the densely populated Osaka-Kyoto corridor in southwest Japan. We investigate how the earthquake transferred stress to nearby faults, altering their proximity to failure and thus changing earthquake probabilities. We find that relative to the pre-Kobe seismicity, Kobe aftershocks were concentrated in regions of calculated Coulomb stress increase and less common in regions of stress decrease. We quantify this relationship by forming the spatial correlation between the seismicity rate change and the Coulomb stress change. The correlation is significant for stress changes greater than 0.2–1.0 bars (0.02–0.1 MPa), and the nonlinear dependence of seismicity rate change on stress change is compatible with a state- and rate-dependent formulation for earthquake occurrence. We extend this analysis to future mainshocks by resolving the stress changes on major faults within 100 km of Kobe and calculating the change in probability caused by these stress changes. Transient effects of the stress changes are incorporated by the state-dependent constitutive relation, which amplifies the permanent stress changes during the aftershock period. Earthquake probability framed in this manner is highly time-dependent, much more so than is assumed in current practice. Because the probabilities depend on several poorly known parameters of the major faults, we estimate uncertainties of the probabilities by Monte Carlo simulation. This enables us to include uncertainties on the elapsed time since the last earthquake, the repeat time and its variability, and the period of aftershock decay. We estimate that a calculated 3-bar (0.3-MPa) stress increase on the eastern section of the Arima-Takatsuki Tectonic Line (ATTL) near Kyoto causes fivefold increase in the 30-year probability of a subsequent large earthquake near Kyoto; a 2-bar (0.2-MPa) stress decrease on the western section of the ATTL results in a reduction in probability by a factor of 140 to 2000. The probability of a Mw = 6.9 earthquake within 50 km of Osaka during 1997–2007 is estimated to have risen from 5–6% before the Kobe earthquake to 7–11% afterward; during 1997–2027, it is estimated to have risen from 14–16% before Kobe to 16–22%.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/98JB00765","issn":"01480227","usgsCitation":"Toda, S., Stein, R., Reasenberg, P., Dieterich, J.H., and Yoshida, A., 1998, Stress transferred by the 1995 Mw = 6.9 Kobe, Japan, shock: Effect on aftershocks and future earthquake probabilities: Journal of Geophysical Research B: Solid Earth, v. 103, no. 10, p. 24543-24565, https://doi.org/10.1029/98JB00765.","productDescription":"23 p.","startPage":"24543","endPage":"24565","numberOfPages":"23","costCenters":[],"links":[{"id":489840,"rank":2,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1029/98jb00765","text":"Publisher Index Page"},{"id":231032,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"103","issue":"10","noUsgsAuthors":false,"publicationDate":"1998-10-10","publicationStatus":"PW","scienceBaseUri":"505b9b69e4b08c986b31ce7c","contributors":{"authors":[{"text":"Toda, S.","contributorId":102228,"corporation":false,"usgs":true,"family":"Toda","given":"S.","email":"","affiliations":[],"preferred":false,"id":386865,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stein, R.S.","contributorId":8875,"corporation":false,"usgs":true,"family":"Stein","given":"R.S.","email":"","affiliations":[],"preferred":false,"id":386861,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Reasenberg, P.A.","contributorId":19959,"corporation":false,"usgs":true,"family":"Reasenberg","given":"P.A.","email":"","affiliations":[],"preferred":false,"id":386862,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Dieterich, James H.","contributorId":81614,"corporation":false,"usgs":true,"family":"Dieterich","given":"James","middleInitial":"H.","affiliations":[],"preferred":false,"id":386864,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Yoshida, A.","contributorId":60807,"corporation":false,"usgs":true,"family":"Yoshida","given":"A.","email":"","affiliations":[],"preferred":false,"id":386863,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":54867,"text":"wdrNY971 - 1998 - Water Resources Data, New York, Water Year 1997; Volume 1. Eastern New York; Excluding Long Island","interactions":[],"lastModifiedDate":"2019-05-14T10:37:17","indexId":"wdrNY971","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"NY-97-1","title":"Water Resources Data, New York, Water Year 1997; Volume 1. Eastern New York; Excluding Long Island","docAbstract":"Water resources data for the 1997 water year for New York consist of records of stage, discharge, and water quality of streams; stage, contents, and water quality of lakes and reservoirs; ground-water levels; and precipitation quality. This volume contains records for water discharge at 117 gaging stations; stage only at 9 gaging stations; stage and contents at 4 gaging stations, and 18 other lakes and reservoirs; water quality at 35 gaging stations and 1 precipitation-quality station; and water levels at 5 observation wells. Also included are data for 38 crest-stage partial-record stations. Locations of all these sites are shown on figure 8. Additional water data were collected at various sites not involved in the systematic data-collection program, and are published as miscellaneous measurements and analyses.These data together with the data in volumes 2 and 3 represent that part of the National Water Data System operated by the U.S. Geological Survey in cooperation with State, Municipal, and Federal agencies in New York.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wdrNY971","collaboration":"Prepared in cooperation with the State of New York and with other agencies","usgsCitation":"Butch, G.K., Lumia, R., and Murray, P.M., 1998, Water Resources Data, New York, Water Year 1997; Volume 1. Eastern New York; Excluding Long Island: U.S. Geological Survey Water Data Report NY-97-1, xvi, 349 p., https://doi.org/10.3133/wdrNY971.","productDescription":"xvi, 349 p.","costCenters":[],"links":[{"id":363749,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wdr/1997/ny-97-1/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":173815,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wdr/1997/ny-97-1/report-thumb.jpg"}],"country":"United States","state":"New York","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.25,\n 41\n ],\n [\n -73.1,\n 41\n ],\n [\n -73.1,\n 45\n ],\n [\n -76.25,\n 45\n ],\n [\n -76.25,\n 41\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fb10d","contributors":{"authors":[{"text":"Butch, Gerard K. gkbutch@usgs.gov","contributorId":914,"corporation":false,"usgs":true,"family":"Butch","given":"Gerard","email":"gkbutch@usgs.gov","middleInitial":"K.","affiliations":[],"preferred":true,"id":251826,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lumia, Richard rlumia@usgs.gov","contributorId":4579,"corporation":false,"usgs":true,"family":"Lumia","given":"Richard","email":"rlumia@usgs.gov","affiliations":[],"preferred":true,"id":251824,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Murray, Patricia M. pmurray@usgs.gov","contributorId":4863,"corporation":false,"usgs":true,"family":"Murray","given":"Patricia","email":"pmurray@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":251825,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":44311,"text":"ofr97102 - 1998 - Hydrogeology and water quality of the Clinton Street-Ballpark Aquifer near Johnson City, New York","interactions":[],"lastModifiedDate":"2017-04-06T11:08:21","indexId":"ofr97102","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"97-102","title":"Hydrogeology and water quality of the Clinton Street-Ballpark Aquifer near Johnson City, New York","docAbstract":"The Clinton Street-Ballpark aquifer, in the Susquehanna River valley in southern Broome County, N.Y., supplies drinking water to the Village of Johnson City near Binghamton. The hydrogeology and water quality of the aquifer were studied in 1994-95 to identify the source area of 1,1,1-trichloroethane, which was detected at the Johnson City Camden Street wellfield in 1991.
The aquifer is generally 100 to 150 ft thick and consists primarily of ice-contact deposits of silty sand and gravel that are overlain by outwash deposits of sand and gravel. These two types of deposits are separated by lacustrine silt and clay of variable thickness into an upper and a lower layer of the aquifer. The coarse deposits form a single aquifer in areas where the lacustrine deposits are absent.
Synoptic water-level surveys indicated that ground water moves from upgradient areas flanking the aquifer boundaries toward two major pumping centers?the Anitec wellfield in Binghamton and the Camden Street wellfield in Johnson City. Areas contributing recharge to municipal and industrial wells in the aquifer were delineated by a previously developed groundwater- flow model. The residence time of ground water within the area contributing recharge to Johnson City well no. 2 in the Camden Street wellfield was estimated to be less than 6 years.
1,1,1-Trichloroethane, trichloroethene, and their metabolites were detected in ground water at several locations in and near Johnson City. Relatively high concentrations of 1,1,1-trichloroethane were found in ground water about 3,000 ft north of the Camden Street wellfield. The suspected source is an area bordered on the south by Field Street, on the north by Harry L. Drive, on the east by New York State Route 201, and on the west by Marie Street. A trichloroethene metabolite, cis-1,2-dichloroethene, appears to be migrating westward from U.S. Air Force Plant 59 toward the Camden Street well-field, 1,000 ft southwest of the plant, although this compound has not been detected in water pumped by municipal wells, possibly because it has become diluted by ground water from other locations within the contributing area to the wells.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr97102","collaboration":"Prepared in cooperation with the U.S. Air Force","usgsCitation":"Coon, W.F., Yager, R.M., Surface, J.M., Randall, A.D., and Eckhardt, D.A., 1998, Hydrogeology and water quality of the Clinton Street-Ballpark Aquifer near Johnson City, New York: U.S. Geological Survey Open-File Report 97-102, Report: 63 p.; 5 Plates, https://doi.org/10.3133/ofr97102.","productDescription":"Report: 63 p.; 5 Plates","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":326220,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0102/ofr1997102_plate3.pdf","text":"Plate 3 ","size":"7.52 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1996-0102","linkHelpText":"- Areas contributing ground water to municipal and industrial wells, and travel times of selected flow lines near Johnson, City, N.Y., 1994"},{"id":326221,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0102/ofr1997102_plate4.pdf","text":"Plate 4 ","size":"5.67 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1996-0102","linkHelpText":"- Concentration of 1,1,1- Trichloroethane (1,1,1-TCA) and 1,1-Dichlorethane (1,1-DCA) in ground water, Johnson City, N.Y., 1994–95"},{"id":326218,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0102/ofr1997102_plate1.pdf","text":"Plate 1","size":"7.84 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1996-0102","linkHelpText":" - Location of wells and surface-water measurement sites in Binghamton and Johnson City, N.Y."},{"id":169353,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1997/0102/coverthb.jpg"},{"id":3724,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1997/0102/ofr19970102.pdf","text":"Report","size":"644 KB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1996-0102"},{"id":326219,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0102/ofr1997102_plate2.pdf","text":"Plate 2 ","size":"637 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1996-0102","linkHelpText":"- Water-table and selected ground-water flow directions in the unconfined layer of the Clinton Street-Ballpark aquifer, Broome County, N.Y., May 1995"},{"id":326222,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0102/ofr1997102_plate5.pdf","text":"Plate 5 ","size":"4.37 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1996-0102","linkHelpText":"- Concentrations of 1,1,1-Trichlorethene (TCE) and cis-1,2-Dichloroethene (cis-1,2-DCE) in ground water, Johnson City, N.Y., 1994–95"}],"contact":"Director, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
The Devils Lake Basin is a 3,810-squaremile closed subbasin of the Red River of the North Basin (fig. 1). About 3,320 square miles of the total 3,810 square miles is tributary to Devils Lake. The Devils Lake Basin contributes to the Red River of the North Basin when the level of Devils Lake is greater than 1,459 feet above sea level.
Lake levels of Devils Lake were recorded sporadically from 1867 to 1890. In 1901, the U.S. Geological Survey established a gaging station on Devils Lake. From 1867 through 1998, the lake level has fluctuated between a minimum of 1,400.9 feet above sea level in 1940 and a maximum of 1,444.7 feet above sea level in 1998 (fig. 2). The maximum, which occurred on July 7, 1998, was 22.1 feet higher than the level recorded in February 1993.
The rapid rise in the lake level of Devils Lake since 1993 is in response to abovenormal precipitation and below-normal evaporation from the summer of 1993 through 1998. Because of the rising lake level, more than 50,000 acres of land and many roads around the lake have been flooded. In addition, the water quality of Devils Lake changed substantially in 1993 because of the summer flooding (Williams-Sether and others, 1996). In response to the flooding, the Devils Lake Basin Interagency Task Force, comprised of many State and Federal agencies, was formed in 1995 to find and propose intermediate (5 years or less) flood mitigation options. Current and accurate hydrologic and water-quality information is needed to assess the effectiveness of the flood mitigation options, which include managing and storing water in the Devils Lake Basin, continuing infrastructure protection, and providing an outlet to the Sheyenne River (Wiche, 1998).
As part of the U.S. Army Corps of Engineers Devils Lake emergency outlet feasibility study, the U.S. Geological Survey is modeling lake levels and sulfate concentrations in Devils Lake to simulate operation of an emergency outlet. Accurate simulation of sulfate concentrations in Devils Lake is required to determine potential effects of the outlet on downstream water quality. Historical sulfate concentrations are used to calibrate and verify the model. Most of the Devils Lake water-quality data available before 1998 were obtained from samples collected from the water column about three to four times a year. The samples were collected at one location in each of the Devils Lake major bays (West Bay, Main Bay, East Bay, and East Devils Lake). However, sample collection from only one location in a bay may not give an adequate representation of the water quality of the bay because of factors such as wind, precipitation, temperature, surface- and ground-water inflow, and possible bed-sediment interactions. Thus, spatial variability (the variability within each bay) and temporal variability (the variability with time) of dissolved sulfate need to be determined to evaluate the accuracy of the estimates obtained from the model.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/fs09699","usgsCitation":"Sether, B.A., Vecchia, A.V., and Berkas, W.R., 1998, Spatial and temporal variability of dissolved sulfate in Devils Lake, North Dakota, 1998: U.S. Geological Survey Fact Sheet 096-99, 4 p., https://doi.org/10.3133/fs09699.","productDescription":"4 p.","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":34167,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/1999/0096/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":117918,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/1999/0096/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6fbe","contributors":{"authors":[{"text":"Sether, Bradley A.","contributorId":54985,"corporation":false,"usgs":true,"family":"Sether","given":"Bradley","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":153434,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vecchia, Aldo V. 0000-0002-2661-4401","orcid":"https://orcid.org/0000-0002-2661-4401","contributorId":41810,"corporation":false,"usgs":true,"family":"Vecchia","given":"Aldo","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":153433,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Berkas, Wayne R. wrberkas@usgs.gov","contributorId":425,"corporation":false,"usgs":true,"family":"Berkas","given":"Wayne","email":"wrberkas@usgs.gov","middleInitial":"R.","affiliations":[{"id":5050,"text":"WY-MT Water Science Center","active":true,"usgs":true}],"preferred":true,"id":153432,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":50213,"text":"ofr98570 - 1998 - Level II scour analysis for Bridge 34 (WWINTH00370034) on Town Highway 37, crossing Mill Brook, West Windsor, Vermont","interactions":[],"lastModifiedDate":"2016-08-25T12:43:10","indexId":"ofr98570","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"98-570","title":"Level II scour analysis for Bridge 34 (WWINTH00370034) on Town Highway 37, crossing Mill Brook, West Windsor, Vermont","docAbstract":"This report provides the results of a detailed Level II analysis of scour potential at structure WWINTH00370034 on Town Highway 37 crossing Mill Brook, West Windsor, Vermont (figures 1–8). A Level II study is a basic engineering analysis of the site, including a quantitative analysis of stream stability and scour (FHWA, 1993). Results of a Level I scour investigation also are included in appendix E of this report. A Level I investigation provides a qualitative geomorphic characterization of the study site. Information on the bridge, gleaned from Vermont Agency of Transportation (VTAOT) files, was compiled prior to conducting Level I and Level II analyses and is found in appendix D.
The site is in the New England Upland section of the New England physiographic province in east-central Vermont. The 16.6-mi2 drainage area is in a predominantly rural and forested basin. In the vicinity of the study site, the surface cover is pasture except for the upstream left bank where there is mostly shrubs and brush.
In the study area, Mill Brook has a sinuous channel with a slope of approximately 0.003 ft/ ft, an average channel top width of 52 ft and an average bank height of 5 ft. The channel bed material ranges from sand to cobbles with a median grain size (D50) of 43.4 mm (0.142 ft). The geomorphic assessment at the time of the Level I and Level II site visit on June 5, 1996, indicated that the reach was laterally unstable. Point bars were observed upstream and downstream of this site. Furthermore, slip failure of the bank material was noted downstream at a cut-bank on the left side of the channel across from a point bar.
The Town Highway 37 crossing of Mill Brook is a 37-ft-long, one-lane covered bridge consisting of one 32-foot wood thru-truss span (Vermont Agency of Transportation, written communication, March 23, 1995). The opening length of the structure parallel to the bridge face is 29.6 ft. The bridge is supported by vertical, laid-up stone abutment walls with concrete facing and laid-up stone wingwalls. The channel is skewed approximately 10 degrees to the opening while the opening-skew-to-roadway is zero degrees.
A scour hole 1.5 ft deeper than the mean thalweg depth was observed along the right abutment during the Level I assessment. Scour protection measures at the site included type-3 (less than 48 inches diameter) and type-4 (less than 60 inches diameter) stone fill. Type-3 stone fill was observed along the upstream right bank and along the right abutments. Type-4 stone fill was observed at the upstream end of the upstream right wingwall. Additional details describing conditions at the site are included in the Level II Summary and appendices D and E.
Scour depths and recommended rock rip-rap sizes were computed using the general guidelines described in Hydraulic Engineering Circular 18 (Richardson and Davis, 1995) for the 100- and 500-year discharges. In addition, the incipient roadway-overtopping discharge was determined and analyzed as another potential worst-case scour scenario. Total scour at a highway crossing is comprised of three components: 1) long-term streambed degradation; 2) contraction scour (due to accelerated flow caused by a reduction in flow area at a bridge) and; 3) local scour (caused by accelerated flow around piers and abutments). Total scour is the sum of the three components. Equations are available to compute depths for contraction and local scour and a summary of the results of these computations follows.
There was no contraction scour predicted for any of the modeled flows. Abutment scour at the left abutment ranged from 5.7 to 7.3 ft, while that at the right abutment ranged from 11.6 to 17.7 ft. The worst-case abutment scour occurred at the 500-year discharge. Additional information on scour depths and depths to armoring are included in the section titled “Scour Results.” Scoured-streambed elevations, based on the calculated scour depths, are presented in tables 1 and 2. A cross-section of the scour computed at the bridge is presented in figure 8. Scour depths were calculated assuming an infinite depth of erosive material and a homogeneous particle-size distribution.
It is generally accepted that the Froehlich equation (abutment scour) gives “excessively conservative estimates of scour depths” (Richardson and Davis, 1995, p. 46). Usually, computed scour depths are evaluated in combination with other information including (but not limited to) historical performance during flood events, the geomorphic stability assessment, existing scour protection measures, and the results of the hydraulic analyses. Therefore, scour depths adopted by VTAOT may differ from the computed values documented herein.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Pembroke, NH","doi":"10.3133/ofr98570","collaboration":"Prepared in cooperation with Vermont Agency of Transportation and Federal Highway Administration","usgsCitation":"Boehmler, E.M., and Wild, E.C., 1998, Level II scour analysis for Bridge 34 (WWINTH00370034) on Town Highway 37, crossing Mill Brook, West Windsor, Vermont: U.S. Geological Survey Open-File Report 98-570, iv, 49 p., https://doi.org/10.3133/ofr98570.","productDescription":"iv, 49 p.","costCenters":[],"links":[{"id":175288,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr98570.JPG"},{"id":280042,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1998/0570/report.pdf"}],"country":"United States","state":"Vermont","city":"West Windsor","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a6486","contributors":{"authors":[{"text":"Boehmler, Erick M.","contributorId":96303,"corporation":false,"usgs":true,"family":"Boehmler","given":"Erick","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":240971,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wild, Emily C. 0000-0001-6157-7629 ecwild@usgs.gov","orcid":"https://orcid.org/0000-0001-6157-7629","contributorId":1810,"corporation":false,"usgs":true,"family":"Wild","given":"Emily","email":"ecwild@usgs.gov","middleInitial":"C.","affiliations":[{"id":5081,"text":"Libraries","active":false,"usgs":true}],"preferred":false,"id":240970,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":50170,"text":"ofr98256 - 1998 - Level II scour analysis for Bridge 33 (WWINTH00300033) on Town Highway 30, crossing Mill Brook, West Windsor, Vermont","interactions":[],"lastModifiedDate":"2016-08-25T15:01:20","indexId":"ofr98256","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"98-256","title":"Level II scour analysis for Bridge 33 (WWINTH00300033) on Town Highway 30, crossing Mill Brook, West Windsor, Vermont","docAbstract":"This report provides the results of a detailed Level II analysis of scour potential at structure WWINTH00300033 on Town Highway 30 crossing Mill Brook, West Windsor, Vermont (Figures 1–8). A Level II study is a basic engineering analysis of the site, including a quantitative analysis of stream stability and scour (FHWA, 1993). Results of a Level I scour investigation also are included in appendix E of this report. A Level I investigation provides a qualitative geomorphic characterization of the study site. Information on the bridge, gleaned from Vermont Agency of Transportation (VTAOT) files, was compiled prior to conducting Level I and Level II analyses and is found in appendix D.
The site is in the New England Upland section of the New England physiographic province in east-central Vermont. The 24.9-mi2 drainage area is in a predominantly rural and forested basin. In the vicinity of the study site, the surface cover is pasture upstream of the bridge while the immediate banks have dense woody vegetation. Downstream of the bridge is forested.
In the study area, Mill Brook has an incised, sinuous channel with a slope of approximately 0.004 ft/ft, an average channel top width of 58 ft and an average bank height of 5 ft. The channel bed material ranges from sand to boulder with a median grain size (D50) of 65.7 mm (0.215 ft). The geomorphic assessment at the time of the Level I and Level II site visit on June 5, 1996, indicated that the reach was stable.
The Town Highway 30 crossing of the Mill Brook is a 46-ft-long, one-lane covered bridge consisting of a 40-foot wood-beam span (Vermont Agency of Transportation, written communication, March 23, 1995). The opening length of the structure parallel to the bridge face is 36.3 ft. The bridge is supported by vertical, concrete capped laid-up stone abutments with wingwalls. The channel is skewed approximately 10 degrees to the opening while the opening-skew-to-roadway is zero degrees.
The only scour protection measure at the site was type-2 stone fill (less than 36 inches diameter) along the upstream right bank, the upstream right wingwall, the right abutment and the downstream left wingwall. Additional details describing conditions at the site are included in the Level II Summary and appendices D and E.
Scour depths and recommended rock rip-rap sizes were computed using the general guidelines described in Hydraulic Engineering Circular 18 (Richardson and Davis, 1995) for the 100- and 500-year discharges. In addition, the incipient roadway-overtopping discharge was analyzed since it had the potential of being the worst-case scour scenario. Total scour at a highway crossing is comprised of three components: 1) long-term streambed degradation; 2) contraction scour (due to accelerated flow caused by a reduction in flow area at a bridge) and; 3) local scour (caused by accelerated flow around piers and abutments). Total scour is the sum of the three components. Equations are available to compute depths for contraction and local scour and a summary of the results of these computations follows.
Contraction scour for all modelled flows ranged from 0.0 to 0.1 ft. The worst-case contraction scour occurred at the 500-year discharge. Abutment scour ranged from 6.0 to 16.0 ft. The worst-case abutment scour occurred at the 500-year discharge. Additional information on scour depths and depths to armoring are included in the section titled “Scour Results”. Scoured-streambed elevations, based on the calculated scour depths, are presented in tables 1 and 2. A cross-section of the scour computed at the bridge is presented in figure 8. Scour depths were calculated assuming an infinite depth of erosive material and a homogeneous particle-size distribution.
Usually, computed scour depths are evaluated in combination with other information including (but not limited to) historical performance during flood events, the geomorphic stability assessment, existing scour protection measures, and the results of the hydraulic analyses. Therefore, scour depths adopted by VTAOT may differ from the computed values documented herein.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Pembroke, NH","doi":"10.3133/ofr98256","collaboration":"Prepared in cooperation with Vermont Agency of Transportation and Federal Highway Administration","usgsCitation":"Wild, E.C., and Flynn, R.H., 1998, Level II scour analysis for Bridge 33 (WWINTH00300033) on Town Highway 30, crossing Mill Brook, West Windsor, Vermont: U.S. Geological Survey Open-File Report 98-256, iv, 51 p., https://doi.org/10.3133/ofr98256.","productDescription":"iv, 51 p.","costCenters":[],"links":[{"id":178498,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr98256.JPG"},{"id":280080,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1998/0256/report.pdf"}],"country":"United States","state":"Vermont","city":"West Windsor","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b18e4b07f02db6a7316","contributors":{"authors":[{"text":"Wild, Emily C. 0000-0001-6157-7629 ecwild@usgs.gov","orcid":"https://orcid.org/0000-0001-6157-7629","contributorId":1810,"corporation":false,"usgs":true,"family":"Wild","given":"Emily","email":"ecwild@usgs.gov","middleInitial":"C.","affiliations":[{"id":5081,"text":"Libraries","active":false,"usgs":true}],"preferred":false,"id":240888,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Flynn, Robert H. rflynn@usgs.gov","contributorId":2137,"corporation":false,"usgs":true,"family":"Flynn","given":"Robert","email":"rflynn@usgs.gov","middleInitial":"H.","affiliations":[{"id":405,"text":"NH/VT office of New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":240887,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":6112,"text":"pp1594 - 1998 - Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida","interactions":[{"subject":{"id":50151,"text":"ofr97665 - 1997 - Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida","indexId":"ofr97665","publicationYear":"1997","noYear":false,"title":"Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida"},"predicate":"SUPERSEDED_BY","object":{"id":6112,"text":"pp1594 - 1998 - Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida","indexId":"pp1594","publicationYear":"1998","noYear":false,"title":"Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida"},"id":1}],"lastModifiedDate":"2023-01-04T22:18:49.854105","indexId":"pp1594","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1594","title":"Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida","docAbstract":"This study is part of a larger effort to identify fresh water needs throughout the region and develop a mechanism for basinwide water management. Quantitative estimates of the amount of aquatic habitat in the floodplain in relation to river flow are presented. Plates show streams, lakes, and floodplain forests connected to the main river channel at selected flows; an analysis of long-term flow record in the Apalachicola River; and a review of the literature regarding fishes in floodplains of the Apalachicola River and other rivers of the Eastern United States. Examples show how this report can be used to assess impacts of flow alterations on aquatic habitats and fishes.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1594","usgsCitation":"Light, H.M., Darst, M.R., and Grubbs, J.W., 1998, Aquatic habitats in relation to river flow in the Apalachicola River floodplain, Florida: U.S. Geological Survey Professional Paper 1594, Report: x, 78 p.; 3 Plates: 24.00 x 20.00 inches, https://doi.org/10.3133/pp1594.","productDescription":"Report: x, 78 p.; 3 Plates: 24.00 x 20.00 inches","costCenters":[],"links":[{"id":824,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://fl.water.usgs.gov/Abstracts/pp1594_light.html","linkFileType":{"id":5,"text":"html"}},{"id":108382,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13154.htm","linkFileType":{"id":5,"text":"html"},"description":"13154"},{"id":33169,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1594/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33168,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1594/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33167,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1594/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33166,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1594/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123210,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1594/report-thumb.jpg"}],"country":"United States","state":"Florida","otherGeospatial":"Apalachicola River floodplain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -84.75130445661839,\n 30.716483697451864\n ],\n [\n -85.21017255157646,\n 30.716483697451864\n ],\n [\n -85.21017255157646,\n 29.68059512605774\n ],\n [\n -84.75130445661839,\n 29.68059512605774\n ],\n [\n -84.75130445661839,\n 30.716483697451864\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac5e4b07f02db67a077","contributors":{"authors":[{"text":"Light, Helen M.","contributorId":18355,"corporation":false,"usgs":true,"family":"Light","given":"Helen","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":152139,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Darst, Melanie R.","contributorId":93042,"corporation":false,"usgs":true,"family":"Darst","given":"Melanie","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":152141,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Grubbs, J. W.","contributorId":77139,"corporation":false,"usgs":true,"family":"Grubbs","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":152140,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":6602,"text":"fs05298 - 1998 - Effect of activities at the Idaho National Engineering and Environmental Laboratory on the water quality of the Snake River Plain aquifer in the Magic Valley study","interactions":[],"lastModifiedDate":"2014-04-10T08:46:25","indexId":"fs05298","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":313,"text":"Fact Sheet","code":"FS","onlineIssn":"2327-6932","printIssn":"2327-6916","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"052-98","title":"Effect of activities at the Idaho National Engineering and Environmental Laboratory on the water quality of the Snake River Plain aquifer in the Magic Valley study","docAbstract":"Radiochemical and chemical constituents in wastewater \ngenerated at facilities of the Idaho National Engineering \nand Environmental Laboratory (INEEL) (figure 1) have \nbeen discharged to waste-disposal ponds and wells since \nthe early 1950 s. Public concern has been expressed that \nsome of these constituents could migrate through the \nSnake River Plain aquifer to the Snake River in the Twin \nFalls-Hagerman area Because of these concerns the \nU.S. Department of Energy (DOE) requested that the U.S. \nGeological Survey (USGS) conduct three studies to gain a \ngreater understanding of the chemical quality of water in \nthe aquifer. One study described a one-time sampling \neffort for radionuclides, trace elements, and organic \ncompounds in the eastern part of the A&B Irrigation \nDistrict in Minidoka County (Mann and Knobel, 1990). \nAnother ongoing study involves sampling for tritium from \n19 springs on the north side of the Snake River in the \nTwin Falls-Hagerman area (Mann, 1989; Mann and Low, \n1994). A third study an ongoing annual sampling effort \nin the area between the southern boundary of the INEEL \nand Hagerman (figure 1) (hereafter referred to as the \nMagic Valley study area), is being conducted with the \nIdaho Department of Water Resources in cooperation with \nthe DOE. Data for a variety of radiochemical and \nchemical constituents from this study have been published \nby Wegner and Campbell (1991); Bartholomay, Edwards, \nand Campbell (1992, 1993, 1994a, 1994b); and \nBartholomay, Williams, and Campbell (1995, 1996, \n1997b). Data discussed in this fact sheet were taken from \nthese reports. An evaluation of data collected during the \nfirst four years of this study (Bartholomay Williams, and \nCampbell, 1997a) showed no pattern of water-quality \nchange for radionuclide data as concentrations randomly \nincreased or decreased. The inorganic constituent data \nshowed no statistical change between sample rounds.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/fs05298","usgsCitation":"Bartholomay, R.C., 1998, Effect of activities at the Idaho National Engineering and Environmental Laboratory on the water quality of the Snake River Plain aquifer in the Magic Valley study: U.S. Geological Survey Fact Sheet 052-98, 4 p., https://doi.org/10.3133/fs05298.","productDescription":"4 p.","numberOfPages":"4","costCenters":[],"links":[{"id":286107,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/0052-98/report-thumb.jpg"},{"id":286106,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/0052-98/report.pdf"}],"country":"United States","state":"Idaho","otherGeospatial":"Snake River Plain","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -115.0,42.5 ], [ -115.0,43.5 ], [ -113.0,43.5 ], [ -113.0,42.5 ], [ -115.0,42.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625824","contributors":{"authors":[{"text":"Bartholomay, Roy C. 0000-0002-4809-9287 rcbarth@usgs.gov","orcid":"https://orcid.org/0000-0002-4809-9287","contributorId":1131,"corporation":false,"usgs":true,"family":"Bartholomay","given":"Roy","email":"rcbarth@usgs.gov","middleInitial":"C.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":153002,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":50196,"text":"ofr98537 - 1998 - Level II scour analysis for Bridge 22 (BRADTH00270022) on Town Highway 27, crossing the Waits River, Bradford, Vermont","interactions":[],"lastModifiedDate":"2016-08-25T15:18:33","indexId":"ofr98537","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"98-537","title":"Level II scour analysis for Bridge 22 (BRADTH00270022) on Town Highway 27, crossing the Waits River, Bradford, Vermont","docAbstract":"This report provides the results of a detailed Level II analysis of scour potential at structure BRADTH00270022 on Town Highway 27 crossing the Waits River, Bradford, Vermont (figures 1–8). A Level II study is a basic engineering analysis of the site, including a quantitative analysis of stream stability and scour (FHWA, 1993). Results of a Level I scour investigation also are included in appendix E of this report. A Level I investigation provides a qualitative geomorphic characterization of the study site. Information on the bridge, obtained from Vermont Agency of Transportation (VTAOT) files, was compiled prior to conducting Level I and Level II analyses and is found in appendix D.
The site is in the New England Upland section of the New England physiographic province in east-central Vermont. The 153-mi2 drainage area is in a predominantly rural and forested basin. However, in the vicinity of the study site, the upstream and downstream left banks are suburban and the upstream and downstream right banks are shrub and brushland.
In the study area, the Waits River has an incised, sinuous channel with a slope of approximately 0.0002 ft/ft, an average channel top width of 125 ft and an average bank height of 4 ft. The channel bed material ranges from silt and clay to bedrock with a median grain size (D50) of 0.393 mm (0.00129 ft). The geomorphic assessment at the time of the Level I and Level II site visit on September 7, 1995, indicated that the reach was stable.
The Town Highway 27 crossing of the Waits River is a 109-ft-long, one-lane bridge consisting of a 104-ft steel-truss span (Vermont Agency of Transportation, written communication, March 16, 1995). The opening length of the structure parallel to the bridge face is 99.2 ft. The bridge is supported by vertical, laid-up stone abutments. The channel is skewed approximately 30 degrees to the opening while the opening-skew-to-roadway is zero degrees.
No evidence of scour was observed during the Level I assessment. Scour protection measures at the site included type-2 stone fill (less than 36 inches diameter) along the upstream right and downstream left banks and type-3 stone fill (less than 48 inches diameter) along the left and right abutments. Additional details describing conditions at the site are included in the Level II Summary and appendices D and E.
Scour depths and recommended rock rip-rap sizes were computed using the general guidelines described in Hydraulic Engineering Circular 18 (Richardson and Davis, 1995) for the 100- and 500-year discharges. Total scour at a highway crossing is comprised of three components: 1) long-term streambed degradation; 2) contraction scour (due to accelerated flow caused by a reduction in flow area at a bridge) and; 3) local scour (caused by accelerated flow around piers and abutments). Total scour is the sum of the three components. Equations are available to compute depths for contraction and local scour and a summary of the results of these computations follows.
Contraction scour for all modelled flows ranged from 1.5 to 2.0 ft. The worst-case contraction scour occurred at the 500-year discharge. Abutment scour ranged from 11.8 to 18.8 ft. The worst-case abutment scour occurred at the 500-year discharge. Additional information on scour depths and depths to armoring are included in the section titled “Scour Results.” Scoured-streambed elevations, based on the calculated scour depths, are presented in tables 1 and 2. A cross-section of the scour computed at the bridge is presented in figure 8. Scour depths were calculated assuming an infinite depth of erosive material and a homogeneous particle-size distribution.
It is generally accepted that the Froehlich equation (abutment scour) gives “excessively conservative estimates of scour depths” (Richardson and Davis, 1995, p. 46). Usually, computed scour depths are evaluated in combination with other information including (but not limited to) historical performance during flood events, the geomorphic stability assessment, existing scour protection measures, and the results of the hydraulic analyses. Therefore, scour depths adopted by VTAOT may differ from the computed values documented herein.
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