North-central Arizona Research Articles

Some Lichens from West Fork, Coconino County, Arizona

Some Lichens from West Fork, Coconino County, Arizona

Specific Limits and Distribution of Meadowlarks of the Desert Grassland

THE polytypic Eastern Meadowlark (Sturnella magna) has a breeding range that extends throughout eastern North America westward to Ontario, Nebraska, Texas, and Arizona, and southward through Central and South America as far as northern Brazil. A monotypic sibling species, the Western Meadowlark (Sturnella neglecta), breeds only in western North America eastward to the Great Lakes region, Missouri, and Texas, and southward on the Mexican plateau to northern Jalisco. A poorly differentiated northwestern race, S. neglecta confluenta, is currently recognized by the A.O.U. Check-list (1957). The breeding ranges of these species overlap broadly throughout the north-central United States, from Oklahoma northeastward into Ontario. Their behavioral and ecological interrelationships within this zone of sympatry have been described elsewhere (Lanyon, 1953, 1956, 1957). A similar analysis of their sympatric relationship in the southwestern United States and in Mexico has been delayed because of the (1) considerable confusion that exists even among contemporary ornithologists as to the specific identification of the meadowlarks breeding in these regions and, owing to this confusion, (2) a lack of reliable distributional data for these areas. The Mexican Check-list states, for example, that the southern limits of the breeding ranges of S. neglecta and S. magna lilianae are not known (Miller et al., 1957). The objectives of this paper are (1) to present the specific limits for those populations of the two species that are involved in the area of geographical overlap in the southwestern United States and Mexico, and (2) to summarize the distributional data for this area based on a reexamination of the material currently available. A preliminary discussion of their ecological relationships in this zone is included. A map of the breeding ranges of the populations under consideration here is presented in Figure 1. On the basis of evidence reviewed during this study, the current taxonomic treatment of the breeding populations within the area of geographical overlap in the southwestern United States and in Mexico appears adequate (Miller et al., 1957), with two races of magna and the monotypic neglecta involved. The breeding ranges of the three races appear to be as follows (cf. Figure 1): (1) Sturnella magna lilianae Oberholser breeds from north-central Arizona east to central eastern New Mexico and south to northern Sonora, Chihuahua, and the Big Bend region of Texas; (2) S. magna auropectoralis Saunders breeds from Sinaloa and central Durango southward, intergrading with S. m. alticola south of the area of sympatry;

CORRELATION CHART OF THE PERMIAN FORMATIONS OF NORTH AMERICA: DISCUSSION OF THE GRAND CANYON SECTION

Research Article| May 01, 1962 CORRELATION CHART OF THE PERMIAN FORMATIONS OF NORTH AMERICA: DISCUSSION OF THE GRAND CANYON SECTION W. L FISHER; W. L FISHER Search for other works by this author on: GSW Google Scholar J. E SORAUF J. E SORAUF Search for other works by this author on: GSW Google Scholar Author and Article Information W. L FISHER J. E SORAUF Publisher: Geological Society of America Received: 07 Aug 1961 First Online: 02 Mar 2017 Online ISSN: 1943-2674 Print ISSN: 0016-7606 Copyright © 1962, The Geological Society of America, Inc. Copyright is not claimed on any material prepared by U.S. government employees within the scope of their employment. GSA Bulletin (1962) 73 (5): 649–652. https://doi.org/10.1130/0016-7606(1962)73[649:CCOTPF]2.0.CO;2 Article history Received: 07 Aug 1961 First Online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Facebook Twitter LinkedIn MailTo Tools Icon Tools Get Permissions Search Site Citation W. L FISHER, J. E SORAUF; CORRELATION CHART OF THE PERMIAN FORMATIONS OF NORTH AMERICA: DISCUSSION OF THE GRAND CANYON SECTION. GSA Bulletin 1962;; 73 (5): 649–652. doi: https://doi.org/10.1130/0016-7606(1962)73[649:CCOTPF]2.0.CO;2 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 Callville Formation (Upper Pennsylvanian) and Pakoon Formation (Lower Permian) of northern Arizona constitute an eastward-extending wedge of carbonate rocks that laterally grades into and interfingers with red beds of the Supai Formation. The Callville or its rock equivalents extends to north-central Arizona; the Pakoon extends only to the central part of the Shivwits Plateau. Interfingering relationships of the Hermit and Supai formations in the Shivwits Plateau contrast with the disconformable contact of these formations in north-central Arizona. 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.

Woodchuck Remains in Northern Arizona Caves

Woodchucks, Marmota flaviventris, have been recorded twice in northern Arizona; these were from skeletal remains at archeological sites in the northeastern part of the state (Keet Seel and Woodchuck Cave). Woodchucks are known to be living today no closer than Kane County, Utah. Recent investigations of caves in north-central Arizona, particularly in the Grand Canyon area, have brought to light the remains of woodchucks in five other places and considerably extend the known range of Marmota flaviventris southward, indicating that the species was rather widespread in northern Arizona a few hundred years ago. The dated material found in the archeological sites has been placed as recently as A.D. 1300 and some as far back as A.D. 200 ± one hundred years. The woodchuck localities of Grand Canyon and the Navajo country lie in desert canyons of the Lower Sonoran Life-zone bordering on the Upper Sonoran. Woodchucks today tend to...

Paleozoic Stratigraphy of Part of Northwestern Arizona

Eleven stratigraphic sections were measured along the southwestern margin of the Colorado Plateau, from north-central Arizona to southeastern Nevada. The northwestern sections are thick and consist dominantly of limestones. The southeastern sections are thin and contain much clastic material. The Cambrian rocks, which are almost 2,200 feet thick in extreme southeastern Nevada, wedge to extinction southeastward. They have complex facies relationships resulting from diverse shifting environments during a Lower-Middle Cambrian transgression and a Middle-Upper(?) Cambrian regression. The deposition of primary dolomitic limestones in two types of shallow-water environment is clearly demonstrated. The Ordovician(?) is represented by a thin wedge of dolomitic limestones which occurs only at the northwest. The Upper Devonian Muddy Peak and Martin limestones form a continuous limestone series across the area. In the southeast the Martin truncates the Middle Cambrian Tapeats sandstone and contains basal clastic beds. In the western Grand Canyon area the Martin limestone contains soft, argillaceous limestone beds of Temple Butte lithologic character. The Rogers Spring and Redwall limestones, western and eastern equivalents, are remarkably uniform in thickness and in general lithologic character. They are of Kinderhookian and Osagian age and consist of thick-bedded, light gray, fine-grained, and oolitic limestones with persistent zones of bedded chert. End_Page 503------------------------------ Fig. 1. Outline map of northwestern Arizona showing location of stratigraphic sections. End_Page 504------------------------------ The Callville limestone, as restricted in this study, is entirely Pennsylvanian. It forms an eastward tapering wedge of two members, which intertongues and intergrades with lower Supai redbeds. The limestones were formed during a Late Pennsylvanian, Virgilian, transgression that extended almost across the area. A new formation, the Pakoon limestone, is proposed for the dolomitic limestones conformably overlying the Callville limestone. These dolomitic limestones were deposited in a Wolfcampian regressive phase, which followed the Late Pennsylvanian transgression. They are overlain conformably by cross-bedded sandstones of Supai lithologic character. The pink and gray, cliff-forming, cross-bedded sandstone overlying the Pakoon limestone is designated the Queantoweap sandstone. This formation is not present in the southwestern part of the area, where the Supai is undifferentiated. The southwestern Supai contains many thin limestone beds between red sandstones. The repetition of these limestones with redbeds suggests simple types of cyclothems. The dominant direction of dip of cross-bedding in all formations between the lower Callville limestone and the Coconino sandstone is south and southeast. This suggests that the source of clastic material was on the northwest or north. The possibility is presented that the Supai redbeds were deposited in a wide mud-flat marginal to a clearer-water environment on the north, and that the repeated subsidence of the mud-flat allowed marine water to spread out cross-bedded sandstones, and at times to precipitate thin limestones. The Coconino sandstone is the only formation which thins northwestward. The consistent dominant southward dip of the eolian, wedge-shaped, cross-beds in the formation indicates that the source of the sand was north of the area. The Toroweap formation consists of two gypsiferous members separated by a middle limestone member. It is Leonardian in age. The aridity or semi-aridity of Coconino time persisted during the deposition of the evaporite members of the Toroweap formation. The Kaibab limestone contains many chert-bearing beds and forms steep cliffs above the less conspicuous cliffs of the Toroweap formation. The Kaibab limestone is overlain by redbeds of the Triassic Moenkopi formation.

Nose Plugs from Northern Arizona

In the summer of 1935 it was realized that a large group of sites just to the east of Flagstaff, between the San Francisco Peaks and the Little Colorado River in northcentral Arizona, were in several respects unique. The presence in this northern area of ball court structures similar to those recognized in southern Arizona by Haury and others was the most outstanding single feature. Subsequently, more detailed research revealed additional southern, or Hohokam-like characters in these sites, and a program of several years of extensive excavation and research was undertaken.

PHYSICAL STATUS OF TWO HUNDRED AND NINETEEN PUEBLO INDIAN CHILDREN

A study of the general physical status of 219 Pueblo Indian children who were from 7 to 11 years of age and who lived in eight pueblos or villages was made in the summer and fall of 1934. Six of the villages were in New Mexico, and two were in Arizona. The children had been the subject of anthropometric measurements for three years.1 The Pueblo Indians are a group of agricultural tribes living in villages in north central New Mexico and northeast Arizona. This region is located in the driest and sunniest part of the United States. The altitude is high, varying between 5,000 and 7,000 feet (1,524 and 2,134 meters); the temperature is subject to wide variations both daily and seasonally.2 These people live in houses built of adobe (mud cakes). The rooms are likely to be dark since windows are few. The windows and doors are,

Correlation of the Permian of Southern Utah, Northern Arizona, Northwestern New Mexico, and Southwestern Colorado

The Permian of southern Utah, northern Arizona, northwestern New Mexico, and southwestern Colorado is conceived as bounded below, except in the Grand Canyon, by conformable Pennsylvanian limestone (Callville limestone in the extreme west, an unnamed unit in north-central Arizona, Hermosa formation in San Juan Valley and southwestern Colorado, Magdalena limestone in northwestern New Mexico), and above by unconformable Triassic deposits (Moenkopi formation, Shinarump conglomerate, and Dolores formation, in order from west to east). In the Grand Canyon the underlying beds are Mississippian (Redwall) limestone. Three main types of Permian sequence occur: that of the Grand Canyon, with the Supai formation and Hermit shale (red beds), Coconino sandstone (light-colored, cross-be ded), and Kaibab limestone, named in ascending order; that of Monument Valley and adjacent country north and south, with the Rico formation (red beds and limestone) below and five units above, here treated as parts of the Cutler formation and named in ascending order the Halgaito tongue (red beds), Cedar Mesa sandstone member (light-colored, cross-bedded), Organ Rock tongue (red beds), De Chelly sandstone member (light-colored, cross-bedded), and Hoskinini tongue (red beds); that of southwestern Colorado, with the Rico formation (red beds and limestone) below and the undivided Cutler formation (red beds) above. The relations of these units to one another are shown in a number of cross sections and the earlier nomenclatures are correlated with that used here. Apparently the Permian began ith the widespread deposition of red beds derived from the east, except in the extreme west part of the area where light-colored sands were laid down. In the east a few marine limestones (Rico) interrupted the sequence of red materials, representing incursions of a sea from the east. These first red deposits were followed by light-colored sands coming from the northwest (Cononino, et cetera), which interfingered End_Page 1413------------------------------ with the red materials that still continued to come in from the east. Then marine waters gradually advanced from the west across the western half of the area, depositing chiefly limestone (Kaibab). East of the sea the light-colored sandstones were the chief deposits in a wide zone, and still farther east the red materials prevailed. Finally, the sea withdrew with seeming abruptness and the whole area was exposed to the period of erosion represented by the unconformity at the base of the Triassic.