Miles In Width Research Articles

Errors in the synoptic weather‐charts which cover the Greenland region

Greenland is a very large island with the outline of a human left ear. Its length in a north‐south direction is about 1,600 nautical or 1,800 English miles, and its average breadth about 600 nautical or 750 English miles. Its area is comparable roughly with that part of the United States which is east of the Mississippi River. Save for this elongated outline, Greenland's model is that of an old‐fashioned hunting‐case watch—it is a flattened dome with increasingly steep outward slopes upon its borders. With exception of a marginal ribbon of land usually less than 50 miles in width, Greenland is blanketed by a glacier which everywhere forms its surface (see Fig. 1).

Structure of central part of Sawtooth Range, Montana

Research Article| August 01, 1943 Structure of central part of Sawtooth Range, Montana CHARLES DEISS CHARLES DEISS Search for other works by this author on: GSW Google Scholar GSA Bulletin (1943) 54 (8): 1123–1168. https://doi.org/10.1130/GSAB-54-1123 Article history received: 04 Jan 1943 first online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Twitter LinkedIn Tools Icon Tools Get Permissions Search Site Citation CHARLES DEISS; Structure of central part of Sawtooth Range, Montana. GSA Bulletin 1943;; 54 (8): 1123–1168. doi: https://doi.org/10.1130/GSAB-54-1123 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract The Sawtooth Range is south of Glacier National Park and forms 85 miles of the Rocky Mountain front in northwestern Montana. The range averages 9 miles in width, consists of a broad northeastward-pointing arc, and extends north across the Saypo quadrangle.The sedimentary rocks exposed in the Sawtooth Range are approximately 5500 feet thick, are Paleozoic and Mesozoic in age, and are divided into nine formations: Pagoda and Steamboat (Middle Cambrian), Switchback (Middle and Upper Cambrian), and Devils Glen (Upper Cambrian), unnamed formation (Upper Devonian), Hannan (Mississippian), Ellis (Upper Jurassic), and Kootenai and Colorado (Lower and Upper Cretaceous).Three structural provinces occur in the central part of the Range: an eastern province, characterized by westward-dipping high-angle to moderately low-angle thrusts that increase in number northward; a central province, characterized by closely spaced, westward-dipping, high-angle thrusts, and by drag-folding of the Devonian and Mississippian rocks comprising the imbricated slices; and a western province, characterized by folded, low-angle overthrusts, above which the rocks are compressed into large open folds.The structures were produced by stresses from the west during the Laramide orogeny. The mountains were maturely eroded during the Tertiary, when the east-west courses of the main streams were established. Uplift in the Pliocene? raised the range to its present altitude but did not cause additional deformation. This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

Cypress‐Gum Communities in the Blue Girth Swamp Near Selma, Alabama

Cypress-gum forests are common along the seaward margin of the Coastal Plain from Texas to Virginia. In addition, there are numerous stands in the low backhands of many of the streams in the interior of the southeastern states (Coulter, '04). Throughout the broad alluvial valleys these swamp forests are usually composed of bald cypress (Taxodium distichum) 2 and tupelo gum (Nyssa aquatica), whereas in pineland ponds they include pond cypress (Taxodium ascendens) and swamp black gum (Nyssa biflora) as the predominant species. In the shallow swampy areas of the lower portion of the Gulf Coastal Plain, slash pine (Pinus caribaea) may be an important associate of pond cypress and swamp black gum. Each of these five swampland species has been observed in pure stand. In some areas these species may occur as companion species, especially where pineland streams flow into broad river valleys. The tupelo gum-cypress-swamp black gum and the tupelo gum-cypress forests investigated have been designated as variants of Cover Types Numbers 94 and 95 by the committee on forest types of the Society of American Foresters (Hawley, R. C. et al, '40). The following species have been listed as common associates: red maple (Rufacer drummondii), planer tree (Planera aquatica), pumpkin ash (Fraxinus profunda), water ash (Fraxinus caroliniana), and black gum (Nyssa sylvatica). These forests are of much importance economically since they yield timber crops on annually flooded soils in addition to harboring some of the most valuable and interesting animals indigenous to southern United States. The stands herein reported are located in the Blue Girth Swamp in Dallas County, Alabama. This swamp is approximately 5 miles east of Selma and is in communication with the Alabama River 4 miles southwest of where the swamp is crossed by State Highway Number 14. The swamp is accessible by numerous field roads, the Southern Railroad, and a cable suspension bridge. Each of these approaches lies to the north of State Highway Number 14 (fig. 1). Blue Girth Swamp lies in an elongated basin which is approximately 10 miles in length and averages about one-third of a mile in width. MiVost of the surrounding terrain is under cultivation, the major crops being cotton, corn, and peanuts. The swamp is spring-fed and possesses a nearly continuous hydroperiod. The average annual fluctuation during normal stream flow approximates 3 feet. Following excessive precipitation during April, 1938, the Alabama River experienced a rise of some 10 feet above flood stage with a corresponding rise in the water level of the swamp. Such a water level, however, is unusual in the Blue Girth Swamp. In the swamp, stands of the tupelo gum-cypress complex are characteristic of the deeper waters (2-7 ft.), while samples of the tupelo gum-cypressswamp black gum forest are found along the marginal areas in shallower waters (0-2 ft.). Pure forests of swamp black gum and marshes of bur-reed (Sparganium americanum) are present in the shallow waters south of State Highway Number 14. Contiguous stands of tupelo gum-cypress-swamp black gum, tu1 Contribution from the Botany Department, Tulane University, New Orleans, Louisiana. The authors wish to thank Mrs. Faith P. Mackaness for drawing the map of Blue Girth basin and environs. 2 Nomenclature follows Small's Manual of the Southeastern Flora, 1933.

Franciscan-Knoxville Problem

Franciscan-Knoxville Problem

Offatts Bayou, a Locality with Recurrent Summer Mortality of Marine Organisms

In July, 1939, the writer was called to Galveston to investigate the sudden mortality of marine organisms in Offats Bayou. Since then several trips have been made to the bayou, none longer than a few days. In 1939 I presented an hypothesis to explain the situation, and, since subsequent observations have tended to confirm it, the facts relating to this somewhat peculiar case seem to be worth recording. Offats Bayou is a blind neck or inlet of water on the bay side of Galveston Island, opening into West Galveston Bay. It is shown on the United States Coast and Geodetic Survey chart No. 1282: Galveston Bay and Approaches. It is two and a half miles long and most of it is approximately half a mile wide. The mouth is constricted to less than a quarter of a mile in width and the inner third is set off from the rest of the bayou by a second constriction of about the same width. The channel at the mouth is approximately twelve feet deep, this being the shallowest part of the bayou. At the inner end of the bayou the depth is said to be forty feet in some places. The greatest depth I encountered was thirty feet, but extensive soundings were not made. Mortality has occurred every summer since 1936, except 1940, and was unknown before. These facts were ascertained from residents of the area. I am especially indebted to Mr. J. U. Rogers, who has watched the vagaries of the bayou for several years, and who has cooperated as an observer on the spot since. 1939. The only event seemingly connected with the commencing of mortality was the dredging of the inner end of Offats Bayou for dirt to be used for the west end fill of Galveston. Death of animals in the bayou was not known before that time and has recurred every summer since. Dredging of the bayou has been carried on for many years (see Hopkins 1931, p. 60). Since 1931 the thirty-foot channel at the mouth of the bayou, mentioned by Hopkins, has shoaled up considerably. Mortality occurs very suddenly in the upper end of the bayou in midsummer. I have never been on hand at the precise time but have made observations a few days afterward. Fish, shrimp, oysters and crabs die, and the crabs have been reported to leave the water and crawl ashore. The species referred to is the common Blue Crab, Callinectes sapidus Rathbun, and such action is not normal for that animal. The suddenness with which mortality occurs and the fact that different phyla of animals are affected argues against epidemic disease as the cause of death and conversely indicates some kind of poisoning or chemical change in the environment. The mortality of animals seems to be connected with local disturbances in the water known to the people along the bayou as boils. They have been described to me by several fishermen. Areas up to thirty feet in diameter in the water boil furiously with escaping 'gas. The color of the water in these areas has been variously described as milky, red, and black. In the parlance of fisher631

Elongate intrusions in eastern Connecticut

The Monson (Glastonbury) tonalite gneiss intrudes the Brimfleld (Bolton) schist in two north‐south bands in north‐central Connecticut extending northward into Massachusetts east of the Triassic lowland. The intrusion discussed in this paper, mapped as Glastonbury gneiss on the geologic map of Connecticut (1906), is 40 miles long and averages three miles in width; part of the west‐central portion is cut by Triassic normal faulting. East of this intrusion a second, even narrower, body of similar gneiss parallels it throughout the entire length, and extends northward to the type‐locality of the Monson gneiss in Massachusetts.

Cambrian geography and sedimentation in the central Cordilleran region

Early Paleozoic geography and sedimentation in the Rocky Mountain Basin were influenced by the positive element, Montania, first noted by Willis, and later described and named by Walcott the “Montana Island.” A southern Waucobian sea entered the Great Basin and transgressed northeastward over Utah while a northern sea advanced over southwestern Alberta and southeastern British Columbia. Cascadia was united with Laurentia by Montania which formed a barrier 550 miles in width across the Cordilleran geosyncline. At the beginning of the Albertan the Cordilleran waters invaded the northern and southern parts of Montania from Canada and the Great Basin. The two seas united in northern Idaho and northeastern Washington forming the Idaho strait, and in northern Montana in the Eastern Rocky Mountain Basin. In Middle Cambrian, Montania was a low island whose apex lay in the region of Glacier National Park. The western part of Montania was elevated before the opening of the Croixan when a sea lay to the east in central-western Montana and extended northwest across southern Alberta into the deeper part of the Cordilleran geosyncline in southeastern British Columbia. Montania was elevated slightly before the Ordovician and remained above water until Middle or Late Devonian. Consequently, Middle or Upper Devonian limestone rests nearly conformably upon eroded Middle Cambrian dolomite in northwestern Montana. The climate was warm, humid and uniform throughout the region during most of the Cambrian, but local aridity and possibly lower temperatures may have prevailed during the Croixan.

The Volcanic Zone of Tarawera, New Zealand

the map, roughly in the shape of a narrow wedge whose blunted apex includes Lake Taupo and the group of volcanic mountains: Ngauruhoe (7515 feet), still active; Tongariro (6400 feet), with its Ketetahi spring; and Ruapehu (9175 feet), the latter the highest mountain in the North Island, with a hot lake in its snow-bound crater. From here the sides of the wedge run approximately north-east for 100 miles to the Bay of Plenty, where they touch the coast at Tauranga Harbour and the mouth of the Whakatane River respectively. The whole of this area is an elevated pumice plateau, 1000-1500 feet above sealevel, dotted with numerous large lakes, extinct volcanic cones, and hot springs. Activity is further continued in the sea-bed of the Bay of Plenty between the above-mentioned points; in Whale Island, with its hot springs; Mayor Island, with hot springs and a shining, black, obsidian-lined, extinct crater 5 miles in circumference; and White Island, an active volcano in the solfatara stage with warm water-filled crater half a mile in diameter, where, with hot sulphuric acid springs, is found hydrochloric acid of remarkable strength. A little to the north of the centre of this belt of thermal activity, and along side the lake from which it takes its name, is the town of Rotorua (3000 inhabitants) surrounded by and built amongst?one might almost say built on top of?hundreds of geysers, boiling springs, hot mud volcanoes, fumaroles, steaming lakes, and silica terraces. The many therapeutic waters and wellappointed bath houses of Rotorua are known to visitors from many countries. South-east of Rotorua and at a distance of between 10 and 17 miles, in the heart of the thermal belt, lies a group of mountains, lakes, and valleys, which some fifty-four years ago were the scene of volcanic and thermal upheaval of a magnitude never even remotely approached in Australia or New Zealand during the last five or six hundred years. Appreciation of the present topography and general appearance of the district as portrayed by the accompanying photographs is hardly possible without previous description of the country prior to the convulsions which so drastically reshaped it. Running from north-east to south-west was a mountain group whose three summits known to the Maoris as Wahanga, Ruawahia, and Tarawera, formed a rough, rocky, and much-crevassed plateau 3 miles long by half a mile in width, covered with large angular fragments of trachyte, broken and split up as though by frost. Although undoubtedly of volcanic origin, it seems reasonable to conclude from the state of the rocks and from the dense native forests that clothed the lower slopes, that no eruption of any size had taken place for many hundreds of years. The statement of the Maoris that it had never been known to erupt since they came to New Zealand

Pleistocene gravels of the Cotswold sub-edge plain from Mickleton to the Frome Valley

I. Introduction The district with which this paper is concerned is defined by the rivers Avon and Severn on the north and west and by the escarpment of the Cotswolds from Mickleton to the Frome valley on the east. In the north of the area, the low ground or sub-edge plain which lies between the hills and the Avon is broken by Bredon Hill. This hill is an outlier of the Cotswolds capped by Inferior Oolite and separated from the main escarpment by a broad vale of Lower Lias clay some six miles wide in the north, between Ashton under Hill and Broadway, but narrower towards the southern end, where the outliers of Dumbleton Hill (Middle and Upper Lias) and Oxenton Hill (Middle and Upper Lias with a small capping of Inferior Oolite) occupy some of the space between Bredon Hill and the escarpment. The north and east of this vale is drained northwards by a small stream, the Isbourne, which rises south of Winchcomb and joins the Avon at Evesham. The Carrant and Tirle brooks drain the south-west part of the vale on the south side of Bredon Hill and join the Avon near Tewkesbury. South of Tewkesbury, the sub-edge plain varies from about three to seven miles in breadth and is broken by the Upper and Middle Lias outliers of Churchdown Hill and Robin's Wood Hill. Numerous small streams drain from the Cotswolds to the Severn, the largest being the river Frome, which flows through Stroud to join

Further Studies of the Genus Quiscalus

IN my preceding 'Auk' papers' on the genus Quiscalus, I treated of the grackles of Louisiana and Mississippi. From those States, thanks chiefly to the cooperation of Mr. E. A. Mcllhenny, I have had a sufficient number of breeding males to warrant an attempt to define their ranges and relationships. Reviewing briefly the theories advanced and results obtained: early in the history of what is believed to be their post-glacial rangeextension from Florida and Texas respectively, Stone's and the Bronzed Grackles first met in southern Louisiana and completely merged by interbreeding. The area of intergradation in the State named now averages forty miles in width. North of this zone, which here trends east and west, only aeneus2 occurs; south of it, only stonei and the Florida form, from which it appears to have descended, are found. In the narrow band separating the two typical primary parental forms, complete intergradation occurs. Sometimes this phenomenon is found in a single colony. The relationships of the birds under these conditions seem clear. As we enter Mississippi the problem becomes more complicated. It will be found treated in the fourth of my 'Auk' papers. Here I wish merely to state that the first papers in this series treated of the birds concerned in the most southern area of their intergradation, while in the present paper I consider them in the most northern area of their intergradation. With the passage of time aeneus has extended its range northward through the interior to Slave Lake and from the upper Mississippi valley has swept eastward through New York on a front which now reaches from the lower Hudson valley eastward and northward; while stonei has ranged northward through Cis-Alleghenia to the northern limits of the Carolinian Fauna, including Long Island and the Connecticut valley. As we try to picture the original grackle invasion of this territory we must remember that by no means all of the newcomers were typical of either stonei or aeneus. The study of adequate material from Louisiana, and particularly Mississippi, has given us some conception of the character of the grackle population at the junction of the western with the eastern form. In this area of intergradation pure-blooded individuals are comparatively rare while intermediates

Modes of Retreat of the Pleistocene Ice Sheets

The Pleistocene ice sheets receded by melting, evaporation, and calving in the marginal belt, while the ice surface in the interior was lowered by evaporation and outflowage of ice. The wastage decreased from the edge toward the center. The zone of melting ranged perhaps from 25 to 100 or more miles in width. For the most part the retreating ice sheets had a firm, continuous, gently to steeply rising edge; but especially in transversal valleys, separated by high ridges, there was formed a belt of stagnant ice, rarely, if ever, as much as 10 miles broad. Contrasting of "downwastage" with "recession" has no physical basis.

Studies on the Ecology of Secondary Communities in a Deciduous Forest Area

In connection with a study of the community aspects of the activities of birds in an agricultural area in northern Illinois, the writer became impressed with the fact that no satisfactory classification of the community types found in such an area had ever been set forth. Existing systems of ecological classification have been based largely on studies of primitive communities, and are only partially applicable to an area of this kind. Ecological problems involving secondary communities in which human influence is present as a relatively constant factor have been investigated to some extent by British ecologists (Smith and Crampton, '14; Stapledon and Jenkins, '16; Salisbury, '18; Tansley and Adamson, '26; Godwin, '29; Adamson, '32; Fenton, '34). These studies, however, have been principally botanical, and usually have been carried on in connection with research on pasture problems. Somewhat similar studies have been made in America in connection with the relation of grazing to forest reproduction (Loveridge, '24; Lutz, '30). A foundation has also been laid for an approach to the theoretical side of the problem presented by man-influenced areas in the work of Shelf ord ('12, '35), and Clements ('36). In none of these studies, however, has a classification of the secondary communities in such areas been presented in a way to show their relations to one another and to the primitive communities from which they were derived. The purpose of this paper is two-fold: (1) to present a working basis for the classification of community types existing under agricultural conditions in a formerly forested area; and (2) to consider the relations of the resident avian population of the area to these community types. The territory studied comprises approximately one square mile. It is situated along the Kankakee River, about a mile from the city of Kankakee, and includes a small portion of the suburban village of Bourbonnais. The part of the area nearest the river contains low sand ridges of glacial origin, and is dissected by a number of deep ravines, which are cut through the drift into the underlying Niagaran limestone. The topography of the remainder is less broken, and merges imperceptibly into the level plain. The original forest belt along the river at this point was apparently about three-fourths of a mile in width. So far as can be ascertained from presentday remnants, this f orest was red oak-sugar maple in the better-watered

Hurricanes into New England: Meteorology of the Storm of September 21, 1938

T HE hurricane of September last was a whirling, circular storm with very destructive winds spread over a diameter of 200 miles. At its center was the usual calm eye, some 40 miles in breadth. This vortex rushed northward to Long Island and New England with the speed of an express train, augmenting wind velocities to extremes of about 120 miles an hour on the east of the path of the center. The wind drove the sea water with such force that, when added to the rise in sea level due to the low pressure and thrown against the coast, the sea rose io to I5 feet above the expected level, in itself high water, the time being high tide. Towering surges on this combined astronomical tide and storm wave threw the sea to such heights that demolition was general along the exposed coast and hundreds of persons were engulfed and drowned. Flying spray incrusted windows and salt killed vegetation 20 miles inland, and traces were found even 50 miles from the raging sea. Inland, the rivers, already flooded by four days of tropical rains, added to the destruction. The gale, roaring in great gusts over the countryside, broke off or uprooted millions of trees, damaged or destroyed thousands of buildings, and, directly or indirectly, downed nearly 20,000 miles of electric-power and telephone lines. Many people were killed or injured by falling trees, chimneys, or flying debris. The damage was most extensive on the tops and sides of hills. There were also lanes of destruction where particularly vicious gusts, attended perhaps by eddies, had plowed through the woods, breaking off trees or uprooting them from the sodden ground. More than five billion board feet of timber were thrown down, leaf pulp turned white houses green, and leaves that were not blown to pieces were scorched by the beating, desiccating gale. There were some 600 lives lost. The American Red Cross places the deaths at 488, with I00 additional missing, and 1754 more or less injured. The WPA survey1 places the loss of human life at 682. The Red Cross also finds that 93,122 families suffered more or less serious property losses, that 6933 summer dwellings, I99I other dwellings, and 2605 boats were destroyed, also 2369 barns and 7438 other buildings.

The Corona by Reflection from the Moon

THE light from the photosphere of the sun will illuminate not only the hemisphere of the moon facing the sun but also a zone five miles wide beyond the great circle bounding the hemisphere. A further zone five miles in width will be illuminated by those radiations emanating from the corona, if the height of the corona be regarded as equal to one radius of the sun. The intenser light of the relatively low inner corona will fall on a narrow strip of this lunar zone, bordering upon the edge of the surface upon which the photospheric light is falling.

The Relations of Some Native Insects to Introduced Food Plants

VAN DEVENTER (1933) was one of the first to call attention to the changes wrought by civilization on prinmeval communities. His investigations reveal that with the introduction of civilization into primitive areas, the large, slow-multiplying mammals are the first forms to go, and these are followed by much of the climax vegetation and the associated invertebrate forms. Man brings into an area a group of organisms which may be called ecologic campfollowers, and these in turn modify the original communities, change the natural sequence of succession, and may in some instances eliminate the endemic vegetation entirely. The present investigation reveals how certain insects native of North America have managed successfully to meet the changes produced in a primitive area by the invasion of two plant forms introduced into the Western Hemisphere by man. The area studied was a portion of the Canadian River floodplain approximately 15 miles long by 3 miles wide, between Cleveland and McClain Counties, Oklahoma, U.S.A. The centre of the area is 4 miles due west of the University of Oklahoma Campus. The floodplain of the river is unique in many respects. Before the country was opened to settlement in 1889, the floodplain presented a very different picture to that at the present time. Extensive forests grew almost to the water's edge in many places, and on the higher levels were subelimax patches of blue-stem (Andropogon furcatus) prairie, the grass higher than a man's head. The river had water actively flowing during the entire year, and the bed ( sand-bar in local parlance) was less than 150 yd. across. The floodplain originally had three definite levels: the bed of the river, an intermediate pseudo-terrace some 5-8 ft. above the bed, and a true terrace 8-12 ft. above the pseudo-terrace. Civilization has changed this state of things to a remarkable degree. Ploughing and over-grazing of the uplands in the river basin caused a greatly increased run-off, which in turn produced devastating floods. The largest flood occurred in 1906 when torrential rains swelled the waters to a breadth of nearly 5 miles over the area. All of the timber on the pseudo-terrace was swept away (an area three-fourths of a mile to a mile wide and about 7 miles long), and much cutting on the river terrace took place also. As a result a desolate sand bar nearly 2 miles in width, with only drifts of uprooted trees remained.

Pootu, A Lost Island

T nHE island of Pootu, like the other Chu-Shan islands, is part of the Tinghai County of CheKiang province, separated from the mainland by the sea of Chi-tou. The surface is rugged and mountainous, with ten notable peaks, not one of which rises to a thousand feet in height. The island is situated about forty miles east of the Che-Kiang coast. It is four miles long from north to south, and from one to two miles in width, about four square miles in area. The island was inhabited before the days of the Tang dynasty. In the days of the first emperor of Tang, Buddhism was introduced. Many temples were then erected, and later enlarged during the succeeding dynasties. Today it has seventy large temples and 192 small temples and shrines. In recent years, however, the temples have been deteriorating, and parts of the temple buildings are used as hostels for people who go there for the summer. In July and August, there are two direct sailings per week between Shanghai and Pootu, but for the rest of the year there are only two indirect ways of going, one by train from Shanghai to Ningpo, and the other by a steamship from Shanghai to Ningpo. Boats leave Ningpo every morning for Pootu. They make three stops on the way: Chenhai, Tinghai, and Shenchiamen (Figure 1). Between Ningpo and Chenhai, the Yungkiang is bordered on both sides by hundreds of ice-houses (Figure 2). Farmers gather ice from fresh water ponds during the winter months and store it up in straw roofed huts thickly covered over by vines. The ice is sold to fishermen in Tinghai for fish storage during the summer season. Each icehouse is worth about fivehundred dollars on an average. Between Chenhai and Tinghai are many islands which rise sharply out of the water and give the effect of recent

Further Remarks on Quiscalus with a Report on Additional Specimens from Louisiana

THANKS to the continued cooperation of Mr. E. A. McIlhenny I can now speak with some definiteness of the distribution and relationships of the forms of the genus Quiscalu-s in Louisiana. I present these data not alone as a contribution to a wider study of our Grackles but for their bearing on the problem of the methods of intergradation of representative forms. My first paper on this subject has been so long out of print that I make no apology for again presenting a map which, semidiagramatically, shows the distribution of Grackles when nesting and thereby illustrates the important position Louisiana occupies in an attempt to define their relationships and breeding ranges. In a word, all four forms of Grackles breed in that state and it is obvious that whatever we can learn about their intergradations there will be of value in their study elsewhere. It will also promote a clearer understanding of our problem if I restate briefly the facts which have developed thus far: First.-The Florida Grackle (No. 1) and the Bronzed Grackle (No. 4), within the limits of their respective ranges, are stable forms, but in the area between their ranges there is wide variation which eventually results in their complete intergradation. Second.-Both to the northward and westward the Florida Grackle gradually changes into the purple-backed bird for which the name Quiscalus quiscula stonei (No. 2) has been proposed. Third.-The Bronzed Grackle (No. 4) breeds from southern Texas to Newfoundland and Great Slave Lake with slight increase in size and no change in color, but from Louisiana to Massachusetts, wherever its range2 meets that of Stone's Grackle, it intergrades with that form through an intermediate known as Quiscalus quiscula ridgwayi (No. 3). In Louisiana the zone of intergradation is about forty miles in width. In the Lower Hudson Valley, Long Island, and southern New England region it is much wider. Turning now to Louisiana, the only state whence I have sufficient material to determine in some detail the distribution of these birds, the map and distribution table beyond, show that, broadly speaking, the southern part of the state is occupied by stonei, with intergrades toward the Florida Grackle, and in the southeast by occasional specimens of the last-named

Status of the Talladega series in southern Appalachian stratigraphy

Research Article| September 30, 1936 Status of the Talladega series in southern Appalachian stratigraphy GEOFFREY W. CRICKMAY GEOFFREY W. CRICKMAY Search for other works by this author on: GSW Google Scholar GSA Bulletin (1936) 47 (9): 1371–1392. https://doi.org/10.1130/GSAB-47-1371 Article history received: 06 Feb 1936 first online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share MailTo Twitter LinkedIn Tools Icon Tools Get Permissions Search Site Citation GEOFFREY W. CRICKMAY; Status of the Talladega series in southern Appalachian stratigraphy. GSA Bulletin 1936;; 47 (9): 1371–1392. doi: https://doi.org/10.1130/GSAB-47-1371 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract THE TALLADEGA SERIESDISTRIBUTIONThe Talladega series has been traced by the writer from Alabama, where it is typically exposed, across northwest Georgia, into North Carolina and Tennessee. The series occupies a belt, trending northeast, 300 miles in length and 1 to 25 miles in width. The belt is separated in most places from the fossiliferous rocks of the Appalachian Valley and Ridge province, which it borders, by a low-angle thrust fault, the Cartersville fault. To the southeast of the belt lie pre-Cambrian crystalline schists, which in Alabama and Georgia are faulted (Whitestone fault) against the Talladega rocks. Thus, a large part of the belt is a fault block bounded by low-angle faults, which, in general, strike northeast and dip southeast (Fig. 1).ALABAMAThe Talladega series was named by E. A. Smith1 for exposures in the Talladega Hills, Alabama (locality 1, Fig. 1). The series2 consists typically of slate . . . This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

An Annotated List of the Birds of Rooks County, Kansas, and Vicinity

The following annotated list of birds is the result of ten years of study and observation in Rooks, Ellis, and Graham counties. For comparison with the records in these counties, studies were also made in Geary, Logan, and Scott counties. The most extensive work was done in Rooks county in 1935 and 1936, in the vicinity of Stockton. Much time was spent in observing and collecting along the south fork of the Solomon river, which runs within a few hundred yards of Stockton on the southwest. Many field trips were taken into the upland prairies. The Solomon river flows east through Rooks county. Its course is marked through most of this county by a winding strip of timber. The principal trees are cottonwood and white elm. The bottomland of this stream averages about one half mile in width. It is largely in cultivation. There are scattered strips, some of them over one fourth mile in width, that are too sandy to farm. Some of this sandy area consists of dunes, where the vegetation is scant and is made up principally of plum brush and prickly pears, with a few scattered hackberry and ash trees. The bluffs bordering the stream rise abruptly on the south to a maximum height of 160 feet above the river. On the north they are of about the same average height, but are not so steep. These bluffs are underlaid with limestone, which crops out along the rims. They are too rocky and rough to cultivate and are nearly all in little bluestem (Andropogon scoparius), which is used for grazing. Above the rims and on the upland prairies buffalo grass (Buchloe dactyloides) is the principal cover where the land is not in cultivation. The bluffs are cut by ravines in which scrubby white elm, ash, and hackberry trees are found (fig. 1). Golden eagles roost in these trees in the winter, while bald eagles are common locally, in the taller trees along the river (fig. 2). Most of the land back of the bluffs is in cultivation and is quite level. There are few trees here excepting those planted around the farm sites and occasional timber claims (fig. 3). The principal crops are wheat, corn, kafir, and cane.

Pleistocene shore lines on the islands of Oahu and Maui, Hawaii

INTRODUCTION Oahu, comprising 598 square miles, and Maui, comprising 728 square miles, are two of the major islands of the Hawaiian group, about 58 miles apart, with Molokai lying between them. Both are volcanic doublets. Oahu is noted for its port of Honolulu, and Maui for its dormant eroded crater of Haleakala. Surrounding Oahu is a narrow coastal plain which emerged from the sea in Pleistocene time, and which, in places, reaches 6 miles in width. It consists of reef limestone and terrigenous deposits. Surrounding all but the east and west ends of Oahu is a fringing reef. Notably different from Oahu is Maui, which has only a few narrow strips of coastal plain, and these contain no reef limestone. The absence of emerged reefs on Maui is, however, not surprising in view of the relative paucity of living reef at the present time. The shore lines described below were . . .