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The Las Vegas Formation

The Las Vegas Formation was established in 1965 to designate the distinctive light-colored, fine-grained, fossil-bearing sedimentary deposits exposed in and around the Las Vegas Valley, Nevada. In a coeval designation, the sediments were subdivided into informal units with stratigraphic and chronologic frameworks that have persisted in the literature. Use of the Las Vegas Formation name over the past half century has been hampered because of the lack of a robust definition and characterization of the entire lithostratigraphic sequence, its geographic distribution, and chronology. This study evaluates and describes deposits attributed to the Las Vegas Formation with detailed stratigraphy, sedimentology, and field relations. A large suite of radiocarbon and luminescence ages facilitates revision and temporal expansion of the geochronology. In all, we characterize 17 informal geologic units within the formation, each dating to a unique period of geologic time, with stratigraphically ascending members X, A, B, D, and E and attendant beds in members B, D, and E. The age of the Las Vegas Formation spans at least the middle Pleistocene to early Holocene (from approximately 573 to 8.53 kilo-annum [thousands of years before present]) and is related to past episodes of groundwater discharge in the Las Vegas Valley. The contextual information derived from this new framework is dually noteworthy because the sediments entomb one of the most significant Pleistocene vertebrate faunas in the American Southwest, the Tule Springs local fauna, and represent a paleohydrologic system that responded dynamically to abrupt changes in climate throughout the late Quaternary. Characterizing the nature of these important deposits stabilizes the nomenclature, promotes the continued use of the informal units within the formation, and facilitates studies of similar deposits associated with desert wetland ecosystems elsewhere in the southwestern United States.

Nevada↗

Groundwater availability of the Williston Basin, United States and Canada

Executive Summary The Williston Basin of the Northern Great Plains is a sedimentary basin—a geologic bowl-like structure filled with layered sedimentary rocks dating as far back as the Paleozoic age. The basin, which is nationally important for the production of energy resources, spans Montana, North Dakota, and South Dakota in the United States, and Manitoba and Saskatchewan in Canada. The three uppermost principal aquifer systems are the glacial, lower Tertiary, and Upper Cretaceous aquifer systems. As deep as 3,000 feet (ft) at the center of the basin, these are the most accessible aquifer systems in the basin and are the primary sources of potable groundwater in much of this area. The glacial aquifer system consists of Quaternary-age unconsolidated till, silt, clay, outwash sand and gravel, and occasional cobbles and boulders. The lower Tertiary and Upper Cretaceous aquifer systems consist primarily of sandstone, siltstone, mudstone, shale, and coal. As energy demands have increased in the basin, horizontal drilling and hydraulic-fracturing have been used (especially since 2005) to develop previously inaccessible formations—namely, the Bakken and Three Forks Formations. The basin has yielded a large supply of domestic oil and natural gas since the 1950s, but the technologies required to extract those materials use large amounts of freshwater. The increasing freshwater demands of energy production in the Williston Basin, in addition to population growth, have led to a need for new tools to assess groundwater resources.

Williston Basin↗

The effects of management practices on grassland birds — An introduction to North American grasslands and the practices used to manage grasslands and grassland birds

The Great Plains of North America is defined as the land mass that encompasses the entire central portion of the North American continent that, at the time of European settlement, was an unbroken expanse of primarily herbaceous vegetation. The Great Plains extend from central Saskatchewan and Alberta to central Mexico and from Indiana to the Rocky Mountains. The expanses of herbaceous vegetation are often referred to as native prairie or native grasslands. Native grasslands share the characteristics of a general uniformity in vegetation structure, dominance by grasses and forbs, a near absence of trees and shrubs, annual precipitation ranging from 25 to 100 centimeters, extreme intra-annual fluctuations in temperature and precipitation, and a flat to rolling topography over which fires can spread. To the west of the Great Plains lie the sagebrush communities of the Great Basin, which extend from British Columbia and Saskatchewan to northern Arizona and New Mexico and from the eastern slopes of the Sierra Nevada and Cascade mountain ranges to western South Dakota. Sagebrush communities share similar characteristics to native grasslands, but their location east of the Rocky Mountains creates a more moderating influence from prevailing westerly winds that affect timing of peak precipitation and growth form of dominant vegetation. Native grasslands and sagebrush communities harbor a diverse array of grassland, wetland, and woodland plant and animal communities that are uniquely adapted to the natural forces of the Great Plains and Great Basin, namely the interactive forces of climate, fire, and grazing. The arrival of European settlers to North America brought profound change to native grassland and sagebrush communities, including the establishment of permanent towns and cities, the proliferation of cropland-based agricultural systems, and the suppression of wildfires. The near extirpation of bison by the 1860s paved the way for dramatic changes in the dominant grazers and a shift in the disturbance patterns that historically influenced vegetation structure. The greatest threat to native grasslands and sagebrush communities in modern times is their loss due to conversion to rowcrop agriculture and to urbanization. Concomitant with habitat loss is a precipitous decline in populations of bird species that evolved with, and are uniquely adapted to, the native grassland and sagebrush habitats. Avian population trends are linked strongly to agricultural land use. Besides outright loss of suitable breeding habitat, agricultural practices affect birds through factors such as pesticide exposure, habitat fragmentation, shifts in predator community composition, and occurrence of brood parasites. Bird populations face other stressors, such as loss of habitat to and behavioral avoidance of urbanized areas, roads, and infrastructure associated with energy production. Despite the many anthropogenic changes to North American grassland and sagebrush communities, some bird species are adaptable and opportunistic in their habitat selection and now utilize one or more human-created habitats. Human-created habitats include pastures, hayfields, agricultural terraces, crop buffer strips, field borders, grassed waterways, fencerows, road rights-of-way, airports, reclaimed coal mines, and planted wildlife cover. Fields of seeded grasslands enrolled in Federal long-term set-aside programs, such as the Conservation Reserve Program in the United States and the Permanent Cover Program in Canada, provide important nesting habitat for grassland bird species. The array of habitats used by birds makes habitat and avian management a complex undertaking, and the scale (for example, local, regional, international) at which management actions can be implemented are such that a universal approach to managing grasslands for the conservation of the entire suite of bird species does not exist. Experienced land managers recognize that it is impossible to manage for all bird species simultaneously, and thus, prioritization is necessary towards those habitats or bird species that the manager or management agency ranks highest for a specific region or management unit. The primary tools available for management are burning, grazing, mowing, herbicide application, and idling, but before choosing a particular practice, a manager will want to consider issues of seasonality, intensity, and frequency. Despite the thousands of studies that are cited in this compendium, much remains unknown about the effects of management practices on bird species. The series of species accounts in this compendium review the current state of knowledge regarding management of grassland and sagebrush bird species and summarize information on the effects of management practices on individual species. The accounts do not give definitive statements on the effects of management practices for any particular species, primarily because there are very few replicated studies in which identical management practices have been applied in the same geographical area with consistent results, which are elements necessary to provide concrete recommendations for the management of a particular species in a particular area. Documentation of the effects of management treatments on individual species through statistically sound methods that incorporate multiple years and locations will further scientists’ and land managers’ knowledge far more than 1–2-year studies that are limited in scope as well as time, but studies of that scope and breadth are rare.

Professional Paper↗

Kīlauea’s 2008–2018 summit lava lake—Chronology and eruption insights

The first eruption at Kīlauea’s summit in 25 years began on March 19, 2008, and persisted for 10 years. The onset of the eruption marked the first explosive activity at the summit since 1924, forming the new “Overlook crater” (as the 2008 summit eruption crater has been informally named) within the existing crater of Halemaʻumaʻu. The first year consisted of sporadic lava activity deep within the Overlook crater. Occasional small explosions deposited spatter and small wall-rock lithic pieces around the Halemaʻumaʻu rim. After a month-long pause at the end of 2008, deep sporadic lava lake activity returned in 2009. Continuous lava lake activity began in February 2010. The lake rose significantly in late 2010 and early 2011, before subsequently draining briefly in March 2011. This disruption of the summit eruption was triggered by eruptive activity on the East Rift Zone. Rising lake levels through 2012 established a more stable, larger lake in 2013, with continued enlargement over the subsequent 5 years. Lava reached the Overlook crater rim and overflowed on the Halemaʻumaʻu floor in brief episodes in 2015, 2016, and 2018, but the lake level was more commonly 20–60 meters below the rim during 2014–18. The lake was approximately 280×200 meters (~42,000 square meters) by early 2018 and formed one of the two largest lava lakes on Earth. A new eruption began in the lower East Rift Zone on May 3, 2018, causing magma to drain from the summit reservoir complex. The lava in Halemaʻumaʻu had drained below the crater floor by May 10, followed by collapse of the Overlook and Halemaʻumaʻu craters. The collapse region expanded as much of the broader summit caldera floor subsided incrementally during June and July. By early August 2018, the collapse sequence had ended, and the summit was quiet. The historical changes in May–August 2018 brought a dramatic end to the decade of sustained activity at Kīlauea’s summit. The unique accessibility of the 2008–18 lava lake provided new observations of lava lake behavior and open-vent basaltic outgassing. Data indicated that explosions were triggered by rockfalls from the crater walls, that the lake consisted of a low-density foamy lava, that cycles of gas pistoning were rooted at shallow depths in the lake, and that lake level fluctuations were closely tied to the pressure of the summit magma reservoir. Lava chemistry added further support for an efficient hydraulic connection between the summit and East Rift Zone. Notwithstanding the benefits to scientific understanding, the eruption presented a persistent hazard of volcanic air pollution (vog) that commonly extended far from Kīlauea’s summit.

Hawaii↗

Views of a century of activity at Kīlauea Caldera—A visual essay

The 2018 eruption of Kīlauea Volcano marked the end of the first sustained period of volcanic activity at Halemaʻumaʻu Crater in 94 years. The views of the lava lake (informally named “Overlook,” nestled within Halemaʻumaʻu) lasted for a decade and seemed timeless. But as we were recently reminded, the summit of Kīlauea is part of a dynamic system that has provided countless new views to observers over the centuries. This visual essay features a few of the many scenes recorded by early observers at the volcano, from the first visits by westerners in 1823 through the explosive eruption of 1924. The early images left by casual visitors, artists, and photographers raise many questions: What is shown? Where is this? Who captured the scene and when? How accurate is the portrayal? Where possible, we attempt to answer these questions and provide interpretations of the images featured. In 1912, the nature of observations at Kīlauea changed when Thomas A. Jaggar, Jr., and others occupied the Hawaiian Volcano Observatory on a full-time basis. They began a visual and written record of what they saw, heard, and experienced that has continued to this day. We describe some of the early work of these scientists and photographers, and showcase the results.

Hawaii↗

Tephra from Kīlauea’s 2008–2018 lava lake eruption—Proximal deposits and dispersal characteristics

A network of ten buckets was established early in the 2008–2018 summit eruption at Kīlauea to collect proximal tephra ejected from the new, informally named the “Overlook crater”; the buckets were emptied on most days of the eruption thereafter. This report summarizes the results of more than 2,400 different sampling intervals (most 1–3 days long) during the eruption, focusing on the physical and dispersal characteristics of the tephra deposits. The network was within about 300 meters south of the vent to capture tephra dispersed by the dominant northeast trade wind. The juvenile tephra mainly reflected spattering at the southeast (SE) sink, a downwelling area in the southeastern part of the lava lake in the Overlook crater that remained in the same area throughout the eruption, with admixtures of solid rock and secondary minerals derived from the wall of the crater. The proportion of juvenile material to lithic material ranged widely early in the eruption but was generally greater than 90 percent for the last 6 years of the eruption as lake level rose and the crater walls decreased in height and became more stable. The accumulation rate of tephra at each bucket was strongly dependent on the location of the bucket and reflects the interplay between lava lake level and wind direction and speed. The mass per unit area (m/a) of collected tephra was a maximum of about 97 kilograms per square meter for the entire eruption, equivalent to a thickness of about 75 millimeters. Thirty-two explosive events with a volcanic explosivity index of −2 to −4 deposited much of the tephra in the network. Fifteen of these rock-fall-induced events occurred within 6 days of one another. Pele’s hair, a volcanic glass predominantly associated with quieter activity at the vent in the final half of the eruption, was dispersed more than 60 kilometers downwind from the lava lake and formed a nearly continuous deposit near the Overlook crater. This eruption was probably the most frequently sampled long-lasting eruption in history, but most of the deposits are ephemeral. The collected samples, although generally of small mass, are retained by the Hawaiian Volcano Observatory and are available for detailed study.

Hawaii↗

The flora of the New Albany shale; Part 2, The Calamopityeae and their relationships

Material referable to Calamopitys americana, Calamopitys foerstei, Stenomyelon muratum, Kalymma lirata, Kalymma resinosa, and Kalymma auriculata, from the upper portion of the New Albany shale in central Kentucky, is described. All these species are based on the internal structure of stems and petioles. The suggestion is made that the genus Stenomyelon should be included in the family Calamopityeae rather than in a separate family. Relationships of the several species and genera belonging to the Calamopityeae are discussed, and it is recommended that the name Calamopitys be restricted to manoxylic forms (C. saturni Unger, etc.), that Eristophyton be used for the pycnoxylic species which have in the past been placed in Calamopitys, and that Sphenoxylon be adopted for the American species which has been called Calamopitys eupunctata. It is pointed out that the Calamopityeae may be divided, naturally, into two major groups-a manoxylic, protostelic group and a pycnoxylic, medullated group. Stenomyelon is probably in the lineage of the more primitive Calamopityeae, and Endoxylon is presumably the most advanced type now known.

Professional Paper↗

Lake Bonneville: Geology of northern Utah Valley, Utah

Lake Bonneville was a vast Pleistocene lake that covered 20,000 square miles in northwestern Utah and had a maximum depth of about 1,000 feet. It was a body of water comparable in size to modern Lake Michigan. Surveys of the unconsolidated deposits in the Lake Bonneville basin utilize the same methods used in studies of hard rocks, namely: separation of the deposits into mappable units and contacts between formations; observations of lateral and vertical changes in lithology; and plotting of these data on the map.

Utah↗

Forest conditions in the Absaroka division of the Yellowstone Forest Reserve, Montana and the Livingston and Big Timber quadrangles

The tract of land here designated the Absaroka division of the Yellowstone Forest Reserve was originally the Absaroka Forest Reserve. By proclamation of January 29, 1903, this reserve was merged with the Teton and the Yellowstone forest reserves, the whole taking the name of the Yellowstone Forest Reserve. The western, northern, and eastern boundaries, as then established and as applicable to the Absaroka division, are as follows: "Beginning at the point where the range line between ranges nine (9) and ten (10) east, principal meridian, Montana, intersects the northern boundary of the Yellowstone National Park; thence northerly along said surveyed and unsurveyed range line, allowing for the proper offset on the first (1st) standard parallel south, to the southwest corner of section eighteen (18), township four (4) south, range ten (10) east; thence easterly to the southeast corner of said section; thence northerly to the northeast corner of section six (6); said township: thence easterly to the southeast corner of section thirty-two (32), township three (3) south, range ten (10) east; thence northerly to the northeast corner of section five (5), said township; thence easterly along the township line to the northeast corner of township three (3) south, range eleven (11) east; thence southerly to the southeast corner of said township; thence easterly along the surveyed and unsurveyed township line to the point for the south- west corner of township three (3) south, range fourteen (14) east; thence northerly along the surveyed and unsurveyed range line to the northwest corner of township two (2) south, range fourteen (14) east; thence easterly to the northeast corner of said township; thence southerly to the point for the southeast corner of said township; thence easterly to the point for the northeast corner of township three (3) south, range fifteen (15) east; thence southerly to the point for the southeast corner of said township; thence easterly along the surveyed and unsurveyed township line to the northwest corner of township four (4) south, range eighteen (18) east; thence southerly along the range line to its intersection with the first (1st) standard parallel south; thence easterly along said parallel to the northeast corner of township six (6) south, range eighteen (18) east; thence southerly along the surveyed and unsurveyed range line to the southwest corner of township seven (7) south, range nineteen (19) east; thence easterly to the northwest comer of township eight (8) south, range twenty (20) east; thence southerly to the southwest corner of said township; thence easterly to the southeast corner of said township; thence southerly along the range line to its intersection with the boundary line between the States of Montana and Wyoming." The southern boundary of the area discussed is west from the point where the eastern boundary of the reserve intersects the Montana- Wyoming line to the southeast corner of township 9 north, range 14 east; thence along the northern boundary line of the Yellowstone National Park to the point where said boundary line of the park intersects the range line between ranges 9 and 10 east, principal meridian. The total area, as above delineated, includes 1,334,400 acres.

Montana↗

Geology of Glacier National Park and the Flathead Region, Northwestern Montana

This report summarizes available data on two adjacent and partly overlapping regions in northwestern Montana. The first of these is Glacier National Park plus small areas east and west of the park. The second is here called, for convenience, the Flathead region; it embraces the mountains from the southern tip of Glacier Park to latitude 48 deg north and between the Great Plains on the east and Flathead Valley on the west. The fieldwork under the direction of the writer was done in 1948, 1949, 1950, and 1951, with some work in 1952 and 1953. The two regions together include parts of the Swan, Flathead, Livingstone, and Lewis Ranges. They are drained largely by branches of the Flathead River. On the east and north, however, they are penetrated by tributaries of the Missouri River and in addition by streams that flow into Canada. Roads and highways reach the borders of the regions; but there are few roads in the regions and only two highways cross them. The principal economic value of the assemblage of mountains described in the present report is as a collecting ground for snow to furnish the water used in the surrounding lowlands and as a scenic and wildlife recreation area. A few metallic deposits and lignitic coal beds are known, but these have not proved to be important and cannot, as far as can now be judged, be expected to become so. No oil except minor seeps has yet been found, and most parts of the two regions covered do not appear geologically favorable to the presence of oil in commercial quantities. The high, Hungry Horse Dam on which construction was in progress during the fieldwork now floods part of the Flathead region and will greatly influence the future of that region. The rocks range in age from Precambrian to Recent. The thickest units belong to the Belt series of Precambrian age, and special attention was paid to them. As a result, it is clear that at least the upper part of the series shows marked lateral changes within short distances. This fact introduces complexities into stratigraphic correlation and should be remembered wherever the series is studied. The stromatolites, or fossil algae, in the Belt series, although still imperfectly understood, give clues with respect to problems of ecology and stratigraphy. The subdivisions of the Belt series within the areas covered by the present report are, in ascending order, Altyn limestone, Appekunny argillite, Grinnell argillite, Siyeh limestone, and Missoula group. Local subdivisions of the Missoula group are possible in certain areas, and all the units just named are expected to be subdivided when detailed studies are undertaken. In the Glacier National Park and Flathead regions together, it is probable that between 25,000 and 30,000 feet of beds belonging to the Belt series, possibly more, are present. These consist largely of quartzitic argillite, quartzite, and carbonate rocks, mostly dolomitic. Small gabbroic and diabasic intrusive bodies and, at one horizon, basaltic lava are associated with the Belt series. Above the Belt series is a thick sequence of Cambrian, Devonian, and Carboniferous strata, in which limestone is dominant, followed by strata of Jurassic and Cretaceous age, largely limestone and shale and partly of terrestrial origin. Slightly consolidated gravel, sand, and silt of Tertiary age are preserved in some valleys and as erosional remnants on the plains close to the mountain border. Pleistocene and Recent glacial and fluviatile deposits are plentiful in mountain valleys and on the plains east of the mountains. Sufficient crustal movements took place during the latter part of Belt time to produce tension cracks that permitted some intrusion and related extrusion to occur. Broad crustal warping probably took place at intervals during the Paleozoic era, but these successive movements left little record other than the absence of sedimentary rock units that might otherwise have been deposited. The same can be said of much of the Me

Professional Paper↗

Synopsis of geologic and hydrologic results: Chapter A in Geological Survey research 1961

The Geological Survey is engaged in many different kinds of investigations in the fields of geology and hydrology. These investigations may be grouped into several broad, inter-related categories as follows: (a) Economic geology, including engineering geology (b) Regional geologic mapping, including detailed mapping and stratigraphic studies (c) Resource and topical studies (d) Ground-water studies (e) Surface-water studies (f) Quality-of-water studies (g) Field and laboratory research on geologic and hydrologic processes and principles. The Geological Survey also carries on investigations in its fields of competence for other Federal agencies that do not have the required specialized staffs or scientific facilities. Nearly all the Geological Survey's activities yield new data and principles of value in the development or application of the geologic and hydrologic sciences. The purpose of this report, which consists of 4 chapters, is to present as promptly as possible findings that have come to the fore during the fiscal year 1961 the 12 months ending June 30, 1961. The present volume, chapter A, is a synopsis of the highlights of recent findings of scientific and economic interest. Some of these findings have been published or placed on open file during the year; some are presented in chapters B, C, and D; still others have not been published previously. Only part of the scientific and economic results developed during the year can be presented in this synopsis. Readers who wish more complete or more detailed information should consult the bibliography of reports beginning on page A-156 of this volume, and the collection of short articles presented in the companion chapters as follows: Prof. Paper 424-B Articles 1 to 146 Prof. Paper 424-C Articles 147 to 292 Prof. Paper 424-D Articles 293 to 435 A list of investigations in progress in the Geologic and Water Resources Divisions with the names and addresses of the project leaders is given on pages A-110 to A-155 for those interested in work in progress in various areas or on special topics. During the fiscal year 1961, the services of the Geologic and Water Resources Divisions were utilized, or supported financially in part, by the many Federal and State agencies listed on pages A-106 to A-109. The Geological Survey has also cooperated from time to time with other agencies, and some of the work described in these chapters stems from work of previous years in cooperation with agencies not shown on the list. All cooperating agencies are identified where appropriate in the individual short articles in chapters B, C, and D, and they are mentioned in connection with some of the larger programs summarized in chapter A; because of space limitations, however, their contributions are mentioned in many of the short summary paragraphs contained in chapter A.

Professional Paper↗

Effects of urban development on direct runoff to East Meadow Brook, Nassau County, Long Island, New York

The study described in this report is concerned with the effects of intensive urban development on direct runoff to East Meadow Brook, a southward-flowing stream in central Nassau County, N.Y., during the period 1937-66. The specific objectives of the study were (a) to relate indices of urban development to increases in the volume of annual direct runoff to the stream; (b) to compare hydrograph features at different periods during the transition of the drainage basin from rural to urban conditions; and (c) to compare the rainfall-runoff relations for periods before and after urban development. Periods of housing and street construction in the drainage basin correspond to three distinct periods of increased direct runoff after the base period 1937-43-namely, 1944-51, 1952-59, and 1960-62. During each period, the average annual direct runoff increased because of an increase in the area served by storm sewers that discharged into East Meadow Brook. The amount of land served by sewers increased from about 570 acres in 1943 to about 3,600 acres in 1962, or about 530 percent. During this same period, the average annual direct runoff increased from about 920 acre-feet per year to about 3,400 acre-feet per year, or about 270 percent. The shape of direct-runoff unit hydrographs of East Meadow Brook also changed during the period of study. The average peak discharge of a 1-hour-duration unit hydrograph increased from 313 cubic feet per second, for storms in 1937-43, to 776 cubic feet per second, for storms in 1960-62, or about 2.5 times. In addition, the widths of the unit hydrographs for 1960-62 at values of 50 and 75 percent of the peak discharge were 38 and 28 percent, respectively, the comparable widths of the unit hydrographs for 1937-43. An analysis of the rainfall-runoff relations for both preurban and urban conditions indicates that the direct runoff for both periods increased with the magnitude of the storm. However, the direct runoff during a period of urbanized conditions (1964- 66) was from 1.1 to 4.6 times greater than the corresponding runoff during the preurban period 1937-43, depending on the size of the individual storm. The volume of direct runoff from the parts of the subarea equipped with storm sewers that discharged into East Meadow Brook is estimated to have been roughly 3,000 acre-feet per year in 1960-62, or about 20 percent of the precipitation on those parts of the area. The increase in direct runoff probably represents a loss of ground-water recharge. However, because data changes in evapo-transpiration are insufficient and because the effects of recharge basins are unknown, adequate quantitative estimates of groundwater recharge can not be made. On the basis of the present zoning regulations and on assumption that an additional 320 acres in the Hempstead subarea will be serviced by storm sewers that discharge into East Meadow Brook, direct runoff from the subarea is expected to increase in the future to an estimated 4,000-4,500 acre-feet per year.

New York↗

History of Snake River Canyon indicated by revised stratigraphy of Snake River Group near Hagerman and King Hill, Idaho

A discovery that debris left by the Bonneville Flood (Melon Gravel) overlies McKinney Basalt about 200 feet above the Snake River near King Hill requires that the stratigraphy of the Snake River Group be revised. In former usage, the McKinney Basalt and its immediately older companion, the Wendell Grade Basalt, were considered on the basis of equivocal field relations to be younger than the Melon Gravel and were assigned to the Recent. These lava flows are here reclassified as Pleistocene. The Bancroft Springs Basalt, which consists of both subaerial lava and pillow lava in a former Snake River canyon, was previously separated from the McKinney but is now combined with the McKinney. Accordingly, the name Bancroft Springs Basalt is here abandoned. This revised stratigraphy is first described from geomorphic relations of the McKinney Basalt near King Hill and is then discussed in the light of drainage changes caused by local lava flows during entrenchment of the Snake River. Near King Hill, a former Snake River canyon was completely filled by McKinney Basalt at the place called Bancroft Springs, hut the depth of this lava in the next several miles of the canyon downstream (along a route that approximately coincides with the present canyon) steadily decreased. This ancestral geomorphology is inferred from the former canyon route and, also, from the continuity in gradient of the McKinney lava surface downstream from Bancroft Springs. The drainage history recorded by various lava flows and river deposits of the Snake River Group indicates that the McKinney and Wendell Grade Basalts erupted after the Snake River canyon had reached its present depth of about 500 feet. The Snake River of that time, as far downstream as Bliss, flowed approximately along its present route. The Wood River of that time, however, skirted the north flank of Gooding Butte and joined the ancestral Snake at a junction, now concealed by lava, north of the present canyon about 3 miles west of Bliss. From that place the former Snake River canyon, also now concealed by lava, continued west to Bancroft Springs and thence along a route close to the present canyon to King Hill. To become entrenched in a canyon 500 feet deep, the Snake River downstream from Hagerman became progressively more incised while its upstream route was pushed south in several earlier canyons by intermittent lava flows. Distinctive gravel deposits help to establish the episodes of progressive canyon cutting and to determine the routes of ancestral drainage, including the former position of the Wood River. As canyon cutting continued, springs began to emerge where lavas had filled the earlier canyons. When the Snake River canyon eventually attained its approximate present depth, the Wendell Grade Basalt erupted near Shoshone and, as several tongues, spread west to the canyon rim opposite Hagerman. One tongue crossed the future route of the Wood River, and another covered an upland area of Sand Springs Basalt that had previously reached the canyon floor at Hagerman. The McKinney Basalt then erupted from McKinney Butte northeast of Bliss and spread southward as a subaerial flow, covering part of the Wendell Grade Basalt. It filled the ancestral Wood River canyon and the Snake River canyon of that time west of Bliss as far downstream as King Hill. The resulting dam of lava impounded a deep lake, which extended upstream in the canyon beyond Hagerman. Copious amounts of the McKinney spilled into this temporary lake and produced pillow lava. About 2 miles west of Bliss, pillow lava 500 feet thick completely fills the former canyon and is protected by rimrock of the subaerial McKinney Basalt. From Bliss, the pillow facies extends upstream as far as the McKinney rimrock - about 5 miles. Eruption of the McKinney Basalt diverted the Wood River to a course along the southeast edge of this lava flow. The temporary lake that was dammed by McKinney Basalt west of Bliss spilled along the sou

Idaho↗

Geologic history of the Colorado River: Chapter C in The Colorado River region and John Wesley Powell (Professional Paper 669)

John Wesley Powell clearly recognized that the spectacular features of the Colorado River - its many grand canyons - were dependent upon the structural history of the mountainous barriers crossed by the river. He conceived of three different historical relationships between rivers and structural features: (1) Newly uplifted land surfaces have rivers that flow down the initial slope of the uplift; these relationships he termed consequent. (2) A river may be older than an uplift that it crosses because it has been able to maintain its course by eroding downward as the uplift progresses; this relationship he named antecedent. (3) An uplifted block may have been buried by younger deposits upon which a river becomes established. The river, in cutting downward, uncovers the uplifted block and becomes incised into it; this relationship he called superimposed. The geologic history of the Colorado River involves all three relationships. In addition, although the position of the river course through a particular structural barrier may have been the result of superposition, the depth of the canyon at that point may be largely due to renewed uplift of the barrier; such deepening of the canyon, therefore, is due to antecedence. The problem of the Colorado River remains today very much as G. K. Gilbert stated it nearly 100 years ago: "How much is antecedent and how much is superimposed?" The question must be asked separately for each stretch of the river.

Colorado River↗

The San Franciscan volcanic field, Arizona

LOCATION OF AREA The San Franciscan volcanic field, which takes its name from San Francisco Mountain, the largest volcano of the group, covers about 3,000 square miles in the north-central part of Arizona, as shown by the shaded space on the index map forming figure 1. The center of the field lies about 50 miles south of the Grand Canyon of the Colorado and the southern boundary is in part coterminous with that of the San Francisco Plateau, which forms the southwestern division of the great Colorado Plateau. The region is easily reached, for the main line of the Atchison, Topeka, & Santa Fe Railway traverses it from east to west for more than 60 miles. Flagstaff, a town of 1,500 inhabitants 10 miles south of the summit of San Francisco Mountain, is on the railroad, amid a branch line runs from Williams, 34 miles farther west, to the Grand Canyon. All the more important points of interest in the field may be reached without difficulty by wagon, and outfits may be obtained at Flagstaff. OUTLINE OF THE REPORT This report deals primarily with the volcanic phenomena of the region as determined in the field and laboratory. Chapter I contains a brief description of the geography of the field and Chapter II is devoted largely to the sedimentary formations and structure. The rest of the report Chapters III to VI—treats entirely of the various features of the volcanoes and igneous rocks, both individually and collectively. Detailed descriptions of the volcanoes and lava fields are given in Chapter III; the volcanic history of the region and its correlation with the general history of the surrounding country are presented in Chapter IV. These two chapters will presumably suffice for the general reader who may desire to become acquainted with the broader volcanic features of the region. Chapter V (Petrography) is devoted entirely to the detailed description of the individual igneous rocks of the region, as represented by a selected set of type specimens. In Chapter VI (Petrology) is presented a discussion of the igneous rocks considered collectively—that is, as a series of genetically related members. These last two chapters will be more especially interesting to petrologists, although there is considerable matter in the last chapter which may also be of interest to the general reader. EXTENT OF FIELD WORK The field work on which the report is based was carried on during the summers of 1901 to 1903, a portion of the time, however, being occupied by side trips to the Grand Canyon of the Colorado, the Verde Valley, and the Moqui Buttes. It was the original intention to study only San Francisco Mountain, but scattered observations made during the first summer at other localities, especially at Elden Mountain and Kendrick Peak, seemed to indicate that the region would repay wider study. The work was accordingly extended so as to embrace all the large cones that lie in the vicinity of San Francisco Mountain and some 2,000 square miles of the surrounding plateau country. The more detailed work was confined to the large cones and the laccoliths, as they presented the greatest variety of phenomena within the smallest space. Reconnaissance work was carried on in the surrounding country more especially for the purpose of determining the limits of the widespread basalt flows, their relation to the underlying sedimentary formations, and the character of those formations.

Arizona↗

Geology of the Sierra Foothills Melange and adjacent areas, Amador County, California

Detailed outcrop mapping in the western Sierra foothills of Amador County, Calif., has resulted in some major changes in the interpretation of stratigraphy and structure. The Amador Group was originally defined at its type locality on the south bank of the Cosumnes River in Amador County to include the Cosumnes Formation and the conformably overlying Logtown Ridge Formation, but the new data indicate that the lower boundary of the type Logtown Ridge should be located 600 m farther west (downsection) than originally designated and that this boundary is a fault. The strata that were originally called the Cosumnes Formation are part of a lithologically diverse assemblage of tectonically intermixed rocks that constitute a newly recognized melange and thus are not a formational rock-stratigraphic unit as the earlier workers believed. Thus, the names Cosumnes Formation and Amador Group are both inappropriate in their type area and are abandoned. The Logtown Ridge Formation is here divided into four members, some of which cross what earlier was considered to be a formational boundary of the Logtown Ridge with overlapping pyroclastic strata. The outcrop mapping requires additional changes, although of lesser importance, in the identification and correlation of other Mesozoic rocks in Amador County. The newly recognized melange forms a 4-km-wide belt underlying the Logtown Ridge Formation. In addition to the type section of the abandoned Cosumnes Formation and scattered fault-bounded blocks of strata of Cosumnes lithology, the melange comprises rocks heretofore mapped as "western belt of Calaveras Formation," considered to be of Paleozoic age. Single clasts of this huge tectonic breccia range from a few centimeters to a few kilometers in maximum dimension. Distinctive strata are generally disrupted, and pervasive shearing is common. In the absence of fossils, no age of original deposition can be assigned to any clast or matrix of the melange, but on the basis of indirect structural evidence, the intermixing that formed the melange probably took place during the Late Jurassic or before, and therefore the now sheared and faulted strata must originally have been at least this old. Available data are ambiguous but suggest that rocks were intermixed to form the melange when the strata were horizontal or nearly so. Similarly, the overlying Logtown Ridge and Mariposa Formations were faulted when these rocks were essentially horizontal. The entire section was subsequently tilted to its present, nearly vertical position. Traditional syntheses of the tectonic history of the Sierra foothills argue that the faults there have always been steeply dipping. Although this may be true for some faults, the new interpretation suggests that most faulting occurred before the section was steeply tilted. Neither suggestion can yet be proved, but we maintain that the highly deformed rocks mapped in Amador County represent primarily the effects of subduction at a continental margin, possibly augmented by gravity tectonics in a trough of sediment accumulation there. On the basis of the ages of affected strata, this period of subduction was Late Jurassic but possibly began at an earlier time. If this interpretation of the melange in Amador County is correct, a belt of similarly deformed rocks should extend far beyond the limits of the study area.

California↗

Post-Carboniferous stratigraphy, northeastern Alaska

Post-Carboniferous sedimentary rocks exposed in northeastern Alaska constitute an almost continuous sequence representing all systems from Permian to Quaternary. Because the rocks are well exposed, only slightly deformed, and very fossiliferous, they comprise an important biostratigraphic reference section. Regional and local unconformities are present, and minor hiatuses can be identified in the stratigraphic record. The rocks are divided into 3 groups, 14 formations, and 16 members; some are newly named, others revised. The Ignek Formation is abandoned, and the Okpikruak Formation is excluded from the stratigraphic sequence in northeastern Alaska. The Sadlerochit Formation is raised to group rank and divided into the Echooka (Permian) and Ivishak (Lower Triassic) Formations. The Echooka includes the Joe Creek and Ikiakpaurak Members (both new), and the Ivishak is divided into the Kavik, Ledge Sandstone, and Fire Creek Siltstone Members (all new). The Shublik Formation (Middle and Upper Triassic) is informally divided into siltstone, limestone and dolomite, and clay shale members; it is separated from the Kingak Shale (Jurrassic) by the (Upper Triassic) Karen Creek Sandstone (new). Lower Cretaceous (Neocomian) rocks are mapped as the Kongakut Formation (new). The Kongakut includes the clay shale, Kemik Sandstone, pebble shale, and siltstone members. The Bathtub Graywacke (new) may be in part equivalent to the Fortress Mountain Formation. The Nanushuk and Colville Groups are extended into northeastern Alaska to replace the Ignek Formation. The Nanushuk includes the Tuktu and Chandler Formations, and the Colville is subdivided into its subordinate Seabee, Prince Creek, and Schrader Bluff Formations. All Tertiary rocks are included in the redefined Sagavanirktok Formation, which is divided into the Sagwon, Franklin Bluffs, and Nuwok Members (new). The Gubik Formation (Pleistocene) is extended into northeastern Alaska. Post-Carboniferous rocks are mainly sandstone, siltstone, shale, and conglomerate, and include both marine and terrestrial deposits with a cumulative thickness of about 8,500 m (28,000 ft). Marine transgressions and regressions are identified in the stratigraphic sequence, and a major shift from a northern source area for the older rocks to a southern source for the younger rocks is demonstrated. This change took place during the Early Cretaceous, and the Bathtub Graywacke is the first unit to clearly reflect a southerly source area. Post-Carboniferous orogeny in northeastern Alaska started during the Aptian Stage of the Lower Cretaceous. Pre-Aptian sandstones are mature, clean, quartz arenites, whereas most post-Aptian sandstones are lithic arenites or graywackes.

Alaska↗

Relation of the Cretaceous formations to the Rocky Mountains in Colorado and New Mexico

Some time ago, while working on a problem that involved the question of the presence or absence of islands near the close of the Cretaceous period in the region now occupied by the southern part of the Rocky Mountains, I was forced to the conclusion that no land masses or islands of any considerable size persisted there throughout the Cretaceous period, for I found no sedimentary rocks that were clearly derived from such islands. This result led to a reexamination of available information to see what evidence the sedimentary rocks in other areas near the present mountains could furnish, and I found rather unexpected confirmation of my conclusion. In the course of this study it became evident t that there is apparent conflict of testimony between different classes of fossils and that the physical evidence, including lithology, structure, and sequence of beds, is at variance with some of the commonly accepted correlations. In this state of uncertainty I tried to apply physiographic principles to see if they would throw any light on the interrelations of the interrelations of the Cretaceous formations of the Rocky Mountain region and on the events that opened and closed the period. This led me to a conclusion similar to that reached by the paleontologist C. A. White many years ago, namely, that the Upper Cretaceous formations up to and including the Laramie extended across the site of the mountains.

Colorado, New Mexico↗