Thesis (M.S.)--Brigham Young University. Dept. of Geography. / Includes bibliographical references (leaves 155-160).

Wellsville Mountain forms the extreme northern end of the Wasatch Range in northern Utah. It lies at the western margin of the Middle Rocky Mountain province and is bordered by valleys of the Basin and Range province. Many geologic investigations have been made in this region. Much of the Wasatch Range has been studied and mapped as well as parts of the Bear River Range, east of Cache Valley, and the Malad Range which extends north from Wellsville Mountain; however, the geology of Wellsville Mountain has not been studied or mapped in detail. Some reconnaissance mapping has been done and sections of Cambrian and Pennsylvanian formations have been measured on the western mountain front (Maxey, 1941; Williams, 1943), but little is known about the middle Paleozoic formations and the structural geology of the northern part of the mountain.

Thesis (D. Min.)--Midwestern Baptist Theological Seminary, 1993. / Includes bibliographical references (leaves 86-88).

The Middle Cambrian Ute Formation includes some 200 m of cyclically alternating carbonates and mud rocks. These are arranged in eight to nine, meter-scale, shallowing-upwards packages, representing deposition under predominantly subtidal conditions. The packages consist of vertical sequences of shale, silty limestone, oncolitic packstone, and oolitic grainstone that exhibit little variance in this general pattern. Small-scale unconformities separate the packages. The inferred depositional environment consists of an intrashelf basin that has a peritidal platform near its margins. The craton, which supplied most of the terrigenous sediment, was situated to the south (Cambrian orientation), and located near the equator. One cycle includes a stromatolite biostrome that is distributed across more than 1500 km2 in northern Utah and southern Idaho. Stromatolites range from mound-like to club-shaped to columnar and reach up to 2 min vertical dimension, and 0.15 min diameter. These large columnar structures were apparently established just basinward of an oolitic shoal. These ancient stromatolites, which are in many ways similar to those stromatolites recently reported from the Bahamas, contain many clues that suggest that they grew in normal marine conditions. These findings require a rethinking of the commonly held belief that Phanerozoic columnar stromatolites are indicators of restricted, hypersaline conditions. Analysis of several orders of laminae in Ute Formation stromatolites indicates periodicity in accumulation from which yearly accumulation rates may be inferred. Values obtained for growth rate range from 4.39-4.88 cm/yr. Such rates of accumulation are in accord with those documented for ancient stromatolites from the Bitter Springs Formation. Thus, even considering the occurrence of hiatal surfaces within the stromatolites, the duration of the columnar-stromatolite horizon probably encompasses 10-2 - 10-3 yr. The biostrome's position in the sequence of cycles and the changes in stromatolite morphology across depositional dip suggest that the biostrome may be essentially isochronous across its outcrop area and, thus, may be viewed as a bioevent horizon. The stromatolites also contribute to a better understanding of the paleogeography of the study area during the Middle Cambrian by providing information on relative energy levels and flow directions. (212 pages)

Wellsville Mountain is 10 miles west of Logan, Utah, at the northern extremity of the Wasatch Range. Paleozoic rocks forma northeast-dipping homocline bounded in part by northwest-trending high-angle faults and cut by a series of northeast-trending high-angle faults. A major transverse fault, with a stratigraphic displacement of 4,500 feet, divides the mountain into two distinct blocks. The rock units of the area are comparable to those of the Logan quadrangle immediately to the east. Pre-Cambrian rocks crop out in Box Elder Canyon, just east of Brigham City, and are overlain by at least 20,000 feet of northeast-dipping Paleozoic rocks of every period except possibly the Permian. The Beirdneau sandstone member of the Jefferson formation, is tentatively correlated with that of the upper Devils Gate limestone of central Nevada. About 6,600 feet of the Oquirrh formation of Pennsylvanian age is exposed near the northern end of Wellsville Mountain. The presence of Desmoinesian fusulinids at the base of the Oquirrh and upper Virgilian fusulinids throughout the interval from 1,000 to 2,000 feet above its base indicates an absence of Lower Pennsylvanian rocks and suggests that the upper 4,400 feet may be in part Permian. Mesozoic rocks are not found in the area. The Wasatch formation and Salt Lake group of Tertiary age crop out in the foothills at the northern end of Wellsville Mountain. Two fault systems are recognized in the area. The northeast-trending high-angle transverse faults of Laramide age and the north-west-trending high-angle bordering faults are Basin and Range age.

The ruffed grouse (Bonasa umbellus incana) inhabits much of the deciduous woodland of northern and central Utah. Its distribution is confined mainly to the Wasatch and Uinta mountain ranges. It has been observed in willows (Salix spp.) at 5, 000 feet elevation and in Douglas-fir (Pseudotsuga menziesii) at 9,000 feet.

Although tabernacles do not hold the sacred meaning of Mormon temples, they are symbolic landmarks of the culture of the early Mormon Saints. Tabernacles were once an integral part of each community in which they were located. They were often the main buildings in the community, reflecting the coherent, orderly nature of a Mormon town. Today, many of the original tabernacles have been torn down and others are under the threat of destruction.The first tabernacles built in the Mormon Culture Region were constructed in the 1850s. They were large meetinghouses built for the purpose of holding large general meetings. They were preacher centered houses of worship with few classrooms or recreational facilities. Over time the tabernacles became larger and often more ornate. Because of the growth of the Church, change in Church programs and technological advancement tabernacles are no longer built. Those remaining are threatened with destruction because of high maintenance costs, and low practicality.

The Nounan Formation in north-central Utah thickens northward from 696 feet near Causey Dam to 1147 feet at High Creek in the Bear River Range, and northwestward to 1149 feet at Dry Canyon in Wellsville Mountain. The basal contact of the Nounan Formation is sharp, but dolomite extends irregularly downward into limestones of the Bloomington Formation as much as 6 feet. The Nounan Formation is divided into three members based on lithologic characters: (1) a lower member composed of dark, medium-crystalline dolomite; (2) a middle member composed of white, coarse-crystalline dolomite with tongues of dark dolomite; and (3) an upper member of interbedded light and dark dolomites and limestones with local arenites and sandy carbonates. The lower member was deposited in a high-energy, shallow-marine subtidal to intertidal environment. Evidence includes sets of low-angle cross stratification (dunes), oncolites, oolites, and rip-up clasts. The middle member forms distinctive ledges and cliffs. The presence of thinly laminated algal stromatolites and relict structures seen also in the lower member indicate a subtidal to intertidal environment similar to that inferred for the lower member. The white color and coarse crystallinity may have resulted from recrystallization of the dark, finer grained dolomite that comprises the lower member. The upper member is characterized by lithologic variability. Thicknesses of limestone are greatest in the north, and decrease to only a few feet in the south. Quartz and other terrigenous minerals are scattered at intervals throughout the upper member, with a marker of sandy (arenaceous) dolomites at the base and near the middle and an increase of sand near the top also. The upper contact, with quartz-rich arenites (subarkosic quartzites) of the Worm Creek Member of tho St. Charles Formation, is gradational overall, but is sharp and planar in each section and readily located. In the upper member, algal mats trapped a varying but overall increasing influx of quartz and feldspar, probably in shallow subtidal environments, and vertically stacked hemispheroids suggest that depositional conditions may have included intertidal. Virtually all of the dolomite in the Nounan Formation must have formed by replacement of lime sediments by downward-moving high-magnesium brines. It is that these brines originated in restricted, shallow, subtidal evaporating basins, such as the Great Bahama Banks today, and associated supratidal flats. Lateral changes from limestone to dolomite overall and also in individual beds of the upper member indicate that the brines travelled laterally as well as vertically, and dolomitization may have been limited as much by prior diagenetic alteration and cementation as by the volume, concentration, and proximity of the brine itself.

Nutritional problems of var ious population groups throughout the world are constantly being emphasized, It has been pointed out that life expectancy at birth is only thirty to forty years for over half of the world's population , while for those people who have been able to take advantage of modern medical and nutritional science, it is sixty five to seventy years, Hunger, as well as preventing economic advancement, promotes unrest and political upheavals. The United States, in the interest of preserving its own security and way of life has a vital stake in solving world nutritional problems as well as its own. Without doubt, we are all aware of this need today of improving the nutritional needs of our own people in practically all parts of the United States. However, the nutritional needs have to be defined before improvements can be recommended. More exact and reliable criteria are needed for identifying borderline cases of malnutrition for various groups of people. This problem is gradually being solved through correlated medical, biochemical, and dietary studies. Thus, as one of the criteria on which to rely, dietary studies are one of the means of measuring the nutritional adequacy of the diet. An evaluation of the school lunch by means of a dietary study cannot be made without also considering the other foods eaten during the day. The benefit of a good school lunch to health and dietary habits, therefore, may be greatest for those children whose family food supplies and habits are the poorest. The benefit will be greatest in the extent to which the foods provided in the school lunch supplement those supplied in the home. A study of the dietary habits of school children in terms of the nutritive value of the school lunch and the rest of the day's food would help to evaluate the nutritional status for the group studied and measure the effectiveness of the school lunch program for improving the dietary habits of the children. Since the school lunch and its contribution tot the total day's diet had not been studied in Utah, seven-day dietary records of the 8th grade Logan Junior High and 8th and 9th grades Wellsville Junior High students were used in evaluating the nutrient intake of the children. The purpose of this study was to determine the contribution of each meal ( breakfast , noon meal , and evening meal) to the total day's diet with emphasis on children eating school lunch versus the children not eating school lunch . The between-meal foods were also studied to see to what extent this supplementary intake improves the overall adequacy of the adolescent's diet .

This study integrates detailed mapping of Tertiary deposits along the divide between the lower Bear River basin and the Cache Valley basin with several other techniques to generate a depositional model, define extension-related structures, and compile a geologic history for this part of the northeastern Basin and Range province. The study area is situated along the topographic divide between Box Elder and Cache Counties, Utah, from the Wellsville Mountains north almost to Clarkston Mountain. These ranges are cored by folded and thrusted Paleozoic rocks. They are bound on the west by normal faults of the Wasatch fault zone and on the east by the West Cache fault zone. Between these two fault zones, poorly consolidated Tertiary deposits of the Wasatch Formation and Salt Lake Formation overlie Paleozoic rocks in the foothills and low divide between the north-trending ranges. The Miocene to Pliocene Salt Lake Formation accumulated above non-tuffaceous conglomerates of the Paleocene to Eocene Wasatch Formation, up to 0.5 km thick in the Wellsville Mountains, but thin or absent northward. The Salt Lake Formation in the study area consists of an apparently non-tuffaceous lower conglomerate member, up to 0.5 km thick in the Wellsville Mountains, and a widespread younger tuffaceous and lacustrine member, at least 1 km thick. The traditional names of Collinston Conglomerate and Cache Valley Member were used for these two lithologies. The Cache Valley Member was further subdivided into a local tuffaceous basal conglomerate, a widespread tuffaceous subunit, and an overlying oolitic subunit. Normal faults in the study area comprise three groups. North-striking normal faults are the youngest, and include major range-bounding faults. East-striking normal faults are less numerous, and are cut by the north-striking faults. The southwest-dipping low-to moderate-angle Beaver Dam fault separates the Cache Butte Divide and Junction Hills from the Wellsville Mountains. It may be unique within the area of study, and may comprise a newly identified segment of the Wasatch fault zone. Most of its displacement appears to pre-date the late Miocene, at the time that previous authors have suggested for the onset of Basin-and-Range normal faulting.