I described the spawning ecology of the Bear Lake Bonneville cutthroat trout (BLBCT) in St. Charles Creek. I tracked cutthroat trout with used radio telemetry. I conducted redd counts to describe spawning conditions. Most cutthroat trout in the Big Arm strayed into the Bear River. Cutthroat trout migrations in the Little Arm and main fork were very limited (<4 km). Redd distributions showed very similar patterns between 1989, 2000 and 2001 with most redds being built in the lowest kilometer of stream. Artificial fish transportation changed the redd distribution in 2002. More redds were built in the main fork and redds were distributed throughout the stream. Redds built in the main fork were characterized by lower levels of fine sediment and higher water velocities as compared to the redds built on the Little Arm. The results of this research will be used to aid resource managers in developing a management plan for wild BLBCT.

Community succession, the orderly changes a community experiences with time, is considered to be the result of either autogenic or allogenic factors working singularly or in combination. It has been further suggested that, as communities undergo succession, certain biological parameters change in a predictable manner. Examination of members 2 through 4 of the Mississippian (KinderhookOsage) Lodgepole Formation of Samaria Mountain, Idaho provides a means to evaluate these concepts. Within the study section comprised of 125 beds (61.5 m thick), four rock types are recognized. These include: (1) fossiliferous wackestone (78% of beds), which ranges in color from dark-gray (N3) to medium-light gray (N6), is fine to coarse crystalline, has an average insoluble content of 3.1 percent by weight, and an average organic content of 0.25 percent by weight; (2) fossiliferous mudstone (1S% of beds), which ranges in color from dark-gray (N3) to medium-gray (NS), is very fine to fine crystalline, has an average insoluble content of 2.3 percent and an average organic content of 0.30 percent by weight; (3) fossiliferous packstone (6% of beds), which ranges in color from medium-gray (NS) to light-gray (N7), is medium to coarse crystalline, has an average insoluble content of 3.3 percent by weight and an average organic content of O. 17 percent by weight; and (4) crystalline carbonate (1% of beds), which is light-gray (N7) in color, is coarse crystalline, has an insoluble content of 9.3 percent by weight, and an organic content of 0.2 percent by weight. However, at ninety-five percent confidence level, no statistical relationship could be seen between the rock types and either the insoluble contents or the organic content. Twenty-one taxa, including corals, brachiopods, crinoids, blastoids, gastropods, echinoids, and sharks were recognized, with most taxa ranging throughout the study section. Well-preserved fossils are generally rare. However, this deficiency seems to be due to weathering of the containing strata rather than to currents acting on the skeletons prior to burial. Orientational data support this conclusion. Measurements of the direction (vector) from the apical end to the calical end of the horn coral Zaphrentis show that the orientations of toppled corals is random. Two biological parameters are calculated for each of the bedding surfaces examined, i.e., diversity and calcified biovolume. Diversity is calculated two ways, i.e., in terms of equitability, and in terms of richness. For richness, values range from 0.0 to 7.41, with a mean of 4.12, and for dominance diversity, values range from 0.0 to 1.95, with a mean value of 0.87. Calcified biovolume, which is used as the basis for inferences involving biomass, ranges from 0 to 30,015 cubic centimeters per bedding surface, with a mean value of 744.1 cubic centimeters per bedding surface. Three faunal associations, as well as several sub-associations within the three major associations, are indicated by the clustering of indices of affinity. These associations include: (1) Zaphrentis-Crinoid- Syringopora-Echinoid-Cleiothryridina-Unispirifer-Spirifer-Orthotetes- Flexaria-Camarotoechia-Schizophoria-Lithostrotionella; (2) Cruziana-Dwelling tube; (3) Shark-Blastoid-Helminthopsis. Trophic relationships within the three associations suggest that they were the result of two factors: (1) the tendency towards a vertical stratification of the association's members, which resulted in a more efficient use of the water column; (2) direct physical interaction among association members, in the form of predator-prey or symbiotic relationships. The former type of interaction may have been operative between the sharks and blastoids of faunal association 3. Environmental reconstruction involved the determination of four parameters: (1) paleocurrent direction and intensity; (2) sedimentation rate; (3) bathymetry; and (4) substrate. From the study of both physical and biological evidence, it is concluded that, during the time of Lodgepole deposition a very weak, unidirectional current, or multidirectional currents of similar competency operated over a carbonate-mud substrate. Evidence suggests that the sedimentati on rate was extremely low, and that the Eh= 0 line was just below the sediment-water interface. The water depth at this location was probably below normal effective wave base, but above the zone of oxygen depletion. Study of fossils on bedding surfaces overlying barren bedding surfaces or surfaces containing fossil hash, suggests that four successional stages can be recognized. Because changes in the faunal composition between the various successional stages appear to take place both with (10 times), and without lithologic changes (16 times), it is concluded that succession may result from either biological modifications of the environment or physical changes. Therefore, succession was both autogenically or allogenically controlled. Additionally, the comnrunities were retrograded to an "earlier" successional stage 24 times within the 125 bed succession. As succession proceeded through the successional sequence, values for equability-diversity and calcified biovolume generally increase. This trend is in agreement with previously predicted trends. With succession the overall trend observed in the trophic structure appears to be one of an increase in the proportion of filter feeders in the community relative to the proportion of deposit feeders in the community.

The Middle Cambrian Ute Formation was studied in the Bear River Range and the Wellsville Mountains of north-central Utah and southeastern Idaho. The depositional textures and sedimentary structures found within the rocks were compared with similar modern sediments and ancient rocks to determine depositional environments, paleogeography, and diagenetic alterations. The rocks of the Ute Formation were divided into five basic types. These five rock types were formed within four identifiable lithofacies: 1) elastic marine shelf; 2) carbonate marine shelf; 3) agitated shoal; and 4) quiet-water shoal. The sequence of elastic and carbonate sediments is believed to have been deposited in a shallow, subtidal environment. Clastic sediments from the east and northwest periodically prograded over the carbonate sequences. A major regression marks the base of the Ute Formation. This was followed by a series of transgressions and regressions, until a major transgression occurred near the end of the deposition of the Ute. Paleomagnetic and faunal evidence suggest the study area was within 10° of the equator during the Middle Cambrian. Clay mineralogy of insoluble residues indicates a humid, tropical climate. Primary diagenetic features are compaction, micritization, and cementation. Secondary diagenetic changes include the inversion of high-magnesium calcite to low-magnesium calcite, aggrading neomorphism, stylolitization, fracturing, and calcite infilling. Partial dolomitization of grains and/or matrix is believed to result from the release of magnesium due to the decomposition of magnesium-rich, organic matter. The formation of a lens-shaped body of dolostone may have resulted from dolomitization by a magnesium-rich fluid circulating along faults.

The Lower Middle Cambrian Langson Formation was studied in the xi Bear River Range of north-central Utah and southeasternmost Idaho and the Wellsville Mountains of north-central Utah. The depositional textures and sedimentary structures preserved within the rocks were compared with characteristics of similar modern sediments and ancient rock to determine environments of deposition, paleogeography, diagenetic alteration and pattern of dolomitization. The rocks of the Langston Formation were divided into eleven different rock types. These eleven rock types were formed within four recognizable lithofacies: 1) upper peritidal; 2) inner carbonate shelf; 3) inner clastic shelf; and 4) outer clastic shelf. The general depositional environment is inferred to have been a shall ow subtidal to subaerial carbonate shoal complex. Clastic sediments from the east and north or northwest periodically prograded over the carbonate complex during times of relatively slow subsidence. The deposition of the Langston Formation mudrocks and carbonates occurred during the first Cambrian grand cycle. Eogenetic diagenetic features include birdseye structures, relict evaporite structures, fibrous rim cement, compaction, and the begining of dolomitization. Mesogenetic diagenesis is characterized by dolomitization and pressure solution. Telogenetic diagenesis is limited to fracturing and calcite infilling. Dolomitization is believed to have resulted mainly from downward reflux of hypersaline brines, as indicated by relict evaporite structures, zoned dolomite rhombs, and a general association of dolomite with upper peritidal facies. The hypersaline brines formed in the upper peritidal environment, and percolated downward through underlying porous sediments. The greater density of the hypersaline brines displaced less-dense interstitial fluids. These brines were periodically diluted by normal marine water or fresh water.

The Swan Peak Formation in the Bear River Range of northern Utah and southeastern Idaho varies in thickness from 0 feet to over 400 feet. It consists of three units: (1) a lower unit of interbedded quartzites, shales, and limestones; (2) A middle unit of interbedded quartzites and shales; (3) An upper unit of nearly homogeneous quartzites. The different sedimentary structures, ichnofossils, body fossils, and mineral compositions of each unit represent different environments of deposition. The lower unit probably was deposited in a shallow-shelf environment, and its sediments grade upward into probably shoreface-, tidal-flat-, and lagoonal deposits of the middle unit. The upper unit is believed to be a shallow-marine sand deposited by south-flowing currents. The lower and middle uits of the Swan Peak Formation consist of a progradational suite of nearshore lithologies formed during the regression of the sea that terminated the early Paleozoic Sauk Sequence. The formation lies disconformably beneath the Ordovician Fish Haven Dolomite, and rests conformably on the underlying Ordovician Garden City Formation. The upper and middle units thin eastward and south-eastward to a feather edge, whereas the lower unit is thickest along an east-west trending belt and thins northward and southward. The lower unit could be time-equivalent to the upper and middle units in the north. Possible estuarine deposits containing detrital hydroxyapatite suggest a local fluvial source in the southeast. The immediate source for much of the sand in the middle and upper units lay northward in Idaho. "Fucoidal markings" within the middle unit appear to be feeding burrows filled with reworked sediment that was consumed or searched for the organic content by littoral to sublittoral benthonic predators or scavengers, probably orthoconic cephalopods.

The purpose of the investigation was to map the geology of the north end of Craters of the Moon National Monument and surrounding area. A stratigraphic sequence of Late Paleozoic sedimentary and Tertiary volcanic rocks was compiles and the structures of these rocks and contact relationships with intrusions were delineated. Grade and facies of contact metamorphism were defined. The Snake River Plain basalts were also mapped. The sources of these flows were determined where possible. Preexisting structures and relationships of vents to earlier faulting were explored in ascertaining extensions of the Great Rift Zone into the Pioneer Mountains. Petrographic descriptions of the rock units were completed. Study of the economic geology was not undertaken. The interested reader is referred to Nelson (1969) for descriptions of the mineral deposits in the Lava Creek Mining District.

As online learning enrollments rapidly increase, it is vital to explore effective course designs that deepen students' learning experiences. This multiple-case study explores four online courses at Brigham Young University–Idaho that include learning activities where students learned through Teach One Another activities. Teach One Another is similar to Reciprocal Peer Learning where students simultaneously learn and contribute to their peers' learning. Findings across the cases of this study show that Teach One Another activities in online courses encourage students to be accountable and motivated to complete individual course work as well as group assignments. As students learn to build trusting learning relationships, group activities may deepen students' learning experiences. This study discusses implications for online course designers, developers, and administrators who are interested in giving students opportunities to deepen their learning of the content and develop life skills such as accountability, responsibility, and trust.

This paper will present a picture of the struggles of the Lemhis prior to and during their residency on the new reservation with a brief follow-up on their ultimate removal to the Fort Hall Reservation. Consideration will be given to the methods by which the Lemhis earned their living, gained their educations, and accomplished their personal conquests. Also included will be accounts of the Nez Perce and Bannock Wars as they related to the Lemhis.

Teton Valley, throughout many centuries, has attracted several occupance groups, each interacting with the environment in various ways for various reasons. Indian and explorer contact did little to alter the surroundings. More frequent contact came, however, as trappers and traders visited the valley to trap beaver and meet in rendezvous.The end of intensified fur trapping slowed contact with the basin. Government personnel, a painter, a few squawmen and horse thieves were the only inhabitants because Indians, remoteness, and harsh climatic conditions kept others out until 1882 when permanent agricultural settlers entered the valley. Hundreds of people followed, many of whom were Mormons from Utah. During this sequence major changes took place. Unique Mormon settlement patterns developed. Increase in agricultural and industrial productivity and population continued until the 1940's, but as enterprises failed people moved out. In the late 1960's the need for a new drawing force was recognized. A ski resort was built, attracting people to the valley to take advantage of the newly created recreational facilities, towns, and businesses.

The Malad Valley is geographically located in a unique position in the Pacific Northwest. The Bear River and its main affluent, the Malad River, are the only rivers in the Pacific Northwest that drain into the Great Basin, whereas the other streams and rivers of the states of Washington, Idaho, and Oregon empty eventually into the Pacific Ocean. It is also characterized for being the northern end of prehistoric Lake Bonneville, and eventually it was through this valley that an outlet opened to drain the lake. The soil deposits from this lake left a fertile valley, capable of producing most crops found in this region.Circumstantial evidence gives indication of many mountain men trapping and exploring in this valley. One account credits Donald McKenzie with naming the Malad River in this valley in 1819 because the flesh of its beaver, when eaten, induced illness in the party. This account, the author found, did not pertain to the Malad River, tributary of the Bear River, but to the other Malad River which is a tributary of the Snake River, over 200 miles distant. Other evidence promotes the idea that the river was named Malade because French trappers became ill from drinking the water. The two Malad Rivers were named for the same reason. Evidence supports the idea that there were two rivers which caused the same ailment when the beaver flesh was consumed. The tributary of the Snake was named by McKenzie and the fur trappers merely referred to another Sick River (Malade), the tributary of the Bear River.