Particel size distribution and microstructures of sediments from ODP Leg 205 sites (Table 1)

Ocean Drilling Program Legs 170 and 205 offshore Costa Rica provide structural observations which support a new model for the geometry and deformation response to the seismic cycle of the frontal sedimentary prism and decollement. The model is based on drillcore, thin section, and electron microscope observations. The decollement damage zone is a few tens of meters in width, it develops mainly within the frontal prism. A clear cm-thick fault core is observed 1.6 km from the trench. The lower boundary of the fault core is coincident with the lithological boundary between the frontal prism and the hemipelagic and pelagic sediment of the Cocos plate. Breccia clast distributions in the upper portion of the decollement damage zone were studied through fractal analysis. This analysis shows that the fractal dimension changes with brecciated fragment size, implying that deformation was not accommodated by self-similar fracturing. A higher fractal dimensionality correlates with smaller particle size, which indicates that different or additional grain-size reduction processes operated during shearing. The co-existence of two distinct fracturing processes is also confirmed by microscopic analysis in which extension fracturing in the upper part of the damage zone farthest from the fault core is frequent, while both extension and shear fracturing occur approaching the fault core. The coexistence of extensional and shear fracturing seems to be best explained by fluid pressure variations in response to variations of the compressional regime during the seismic cycle. During the co-seismic event, sub-horizontal compression and fluid pressure increase, triggering shear fracturing and fluid expulsion. Fractures migrate upward with fluids, contributing to the asymmetric shape of the decollement, while slip propagates. In the inter-seismic interval the frontal prismrelaxes and fluid pressure drops. The frontal prismgoes into diffuse extension during the intervalwhen plate convergence is accommodated by creep along the ductile fault core. The fault core is typically a barrier to deformation, which is explained by its weak, but impermeable, nature. The localized development of a damage zone beneath the fault core is characterized by shear fracturing that appears as the result of local strengthening of the detachment.

Early Cretaceous planktonic foraminifera from the Tethys

Early Cretaceous planktonic foraminiferal assemblages include rare planispiral and pseudoplanispiral morphotypes with elongate chambers that BouDagher-Fadel et al. assigned to Schackoina or accommodated in the new genus Claviblowiella. New findings of well-preserved planktonic foraminiferal faunas from the Lesches en Diois (SE France) section, the Cismon core (NE Italy), the Calabianca (NW Sicily) section and the Upper Aptian of Deep Sea Drilling Project (DSDP) Site 545 drilled off Morocco, have allowed a better understanding of the morphological features of these rare, unevenly distributed taxa. Our data demonstrate that each small planispiral species with globular chambers has a corresponding "clavate" morphotype which (as the "normal" forms) exhibits a smooth, finely perforate wall. Consequently, the latter have been assigned here to the genus Globigerinelloides and treated as subspecies of the "non-clavate" taxa. The (clavate) subspecies belonging to the genus Globigerinelloides here retained are G. duboisi sigali Longoria, G. maridalensis elongatus subsp. nov., G. blowi lobatus subsp. nov. and G. paragottisi clavatus subsp. nov., while Globigerinelloides minai Obregòn de la Parra is not retained. In addition, a new genus, Pseudoschackoina, type species Planomalina saundersi Bolli (senior synonym of Hastigerinoides cepedai Obregòn de la Parra, has been formalised for individuals possessing elongate, pointed, laterally compressed chambers, bearing tubulospines arranged on a pseudoplanispiral (dysaxial) coiling mode. Stratigraphically, in the sections studied the first taxon to appear is Pseudoschackoina saundersi, in the uppermost part of the Selli Level (=OAE1a), immediately followed, just above the OAE1a, by all the "clavate" globigerinelloidids. Regarding the last occurrences, Pseudoschackoina saundersi and G. maridalensis elongatus disappear in the lower part of the Globigerinelloides algerianus Zone, Globigerinelloides paragottisi clavatus at the top of the same zone, while Globigerinelloides blowi lobatus and G. duboisi sigali range up to the lower part of the Ticinella bejaouaensis Zone.

Commencement. Ferry Field

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facililties. By 1914, 13,600 accommodated. New stadium built in 1927. Stamp on verso: Ivory Photo

Ferry Field [Gate at northeast corner]

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facililties. By 1914, 13,600 accommodated. New stadium built in 1927.

Ferry Field. Football. Northeast gate

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facililties. By 1914, 13,600 accommodated. New stadium built in 1927.

Ferry Field [South Bleachers]

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facililties. By 1914, 13,600 accommodated. New stadium built in 1927.

A Football Game on Ferry Field

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facilties. By 1914, 13,600 accommodated. New stadium built in 1927.On image: Printed in Germany

Ferry Field

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facililties. By 1914, 13,600 accommodated. New stadium built in 1927.

Ferry Field [gridiron and track looking west]

Regents purchased south ten acres for $3000 in 1890. In 1902 UM received seven acres of land to the north from Dexter M. Ferry; became Ferry Field. In 1904 brick wall constructed on three sides and in 1906 gate and ticket office at northeast corner added (gift of Mr. Ferry). Wooden stands to accommodate 400 put up in 1893; burned in 1895. Rebuilt to seat 800 with later additions to facililties. By 1914, 13,600 accommodated. New stadium built in 1927.

Evaluation of Potential Post-Glacial Faults Using Bare-Earth LiDAR Topographic Data Near Ridley Island, British Columbia

I present results of my evaluation to identify topographic lineaments that are potentially related to post-glacial faulting using bare-earth LiDAR topographic data near Ridley Island, British Columbia. The purpose of this evaluation has been to review bare-earth LiDAR data for evidence of post-glacial faulting in the area surrounding Ridley Island and provide a map of the potential faults to review and possibly field check. My work consisted of an extensive literature review to understand the tectonic, geologic, glacial and sea level history of the area and analysis of bare-earth LiDAR data for Ridley Island and the surrounding region. Ridley Island and the surrounding north coast of British Columbia have a long and complex tectonic and geologic history. The north coast of British Columbia consists of a series of accreted terranes and some post-accretionary deposits. The accreted terranes were attached to the North American continent during subduction of the Pacific Plate between approximately 200 Ma and 10 Ma. The terrane and post-accretionary deposits are metamorphosed sedimentary, volcanic and intrusive rocks. The rocks have experienced significant deformation and been intruded by plutonic bodies. Approximately 10 Ma subduction of the Pacific Plate beneath the North America Plate ceased along the central and north coast of British Columbia and the Queen Charlotte Fault Zone was formed. The Queen Charlotte Fault Zone is a transform-type fault that separates the Pacific Plate from the North America Plate. Within the past 1 million years, the area has experienced multiple glacial/interglacial cycles. The most recent glacial cycle occurred approximately 23,000 to 13,500 years ago. Few Quaternary deposits have been mapped in the area. The vast majority of seismicity around the northwest coast of British Columbia occurs along the Queen Charlotte Fault Zone. Numerous faults have been mapped in the area, but there is currently no evidence to suggest these faults are active (i.e. have evidence for post-glacial surface displacement or deformation). No earthquakes have been recorded within 50 km of Ridley Island. Several small earthquakes (less than magnitude 6) have been recorded within 100 km of the island. These earthquakes have not been correlated to active faults. GPS data suggests there is ongoing strain in the vicinity of Ridley Island. The strain has the potential to be released along faults, but the calculated strain may be a result of erroneous data or accommodated aseismically. Currently, the greatest known seismic hazard to Ridley Island is the Queen Charlotte Fault Zone. LiDAR data for Ridley Island, Digby Island, Lelu Island and portions of Kaien Island, Smith Island and the British Columbia mainland were reviewed and analyzed for evidence of postglacial faulting. The data showed a strong fabric across the landscape with a northwest-southeast trend that appears to mirror the observed foliation in the area. A total of 80 potential post-glacial faults were identified. Three lineaments are categorized as high, forty-one lineaments are categorized as medium and thirty-six lineaments are categorized as low. The identified features should be examined in the field to further assess potential activity. My analysis did not include areas outside of the LiDAR coverage; however faulting may be present there. LiDAR data analysis is only useful for detecting faults with surficial expressions. Faulting without obvious surficial expressions may be present in the study area.

An Exploratory Assessment of Parklet Usage in Seattle: Methods and Findings

Thesis (Master's)--University of Washington, 2016-06

Analysis of adsorption of gases and vapors on nonporous graphitized thermal carbon black

In this paper we analyzed the adsorption of a large number of gases and vapors on graphitized thermal carbon black. The Henry constant was used to determine the adsorbate-adsorbent interaction energy, which is found to be a modest decreasing function of temperature. Analysis of the complete adsorption isotherm over a wider range of pressure yields information on the monolayer coverage concentration and the adsorbate-adsorbate interaction energy. Among the various equations tested, the Hill-de Boer equation accounting for BET-postulated multilayer formation describes well the adsorption isotherms of all adsorbates. On average, the adsorbate-adsorbate interaction energy in the adsorbed phase is less than that in the bulk phase, suggesting that the distance between adsorbed molecules in the first layer of the adsorbed phase is slightly less than the equilibrium distance between two adsorbate molecules in the bulk phase. This suggests that the first layer is in a compressed state, which is due to the attraction of the adsorbent surface. The monolayer concentration as determined from the fitting of the Hill-de Boer equation with experimental data is slightly larger than the values calculated from the molecular projection area, suggesting that molecules can be oriented such that a larger number of molecules can be accommodated on the carbon black surface. This further supports the shorter distance between adsorbate molecules in the adsorbed phase.

Structure of Petunia hybrida Defensin 1, a Novel Plant Defensin with Five Disulfide Bonds

The structure of a novel plant defensin isolated from the flowers of Petunia hybrida has been determined by H-1 NMR spectroscopy. P. hybrida defensin 1 (PhD1) is a basic, cysteine-rich, antifungal protein of 47 residues and is the first example of a new subclass of plant defensins with five disulfide bonds whose structure has been determined. PhD1 has the fold of the cysteine-stabilized alphabeta motif, consisting of an alpha-helix and a triple-stranded antiparallel beta-sheet, except that it contains a fifth disulfide bond from the first loop to the alpha-helix. The additional disulfide bond is accommodated in PhD1 without any alteration of its tertiary structure with respect to other plant defensins. Comparison of its structure with those of classic, four-disulfide defensins has allowed us to identify a previously unrecognized hydrogen bond network that is integral to structure stabilization in the family.

Differential expression of the GABA transporters GAT-1 and GAT-3 in brains of rats, cats, monkeys and humans

The homeostasis of GABA is critical to normal brain function. Extracellular levels of GABA are regulated mainly by plasmalemmal gamma-aminobutyric acid (GABA) transporters. Whereas the expression of GABA transporters has been extensively studied in rodents, validation of this data in other species, including humans, has been limited. As this information is crucial for our understanding of therapeutic options in human diseases such as epilepsy, we have compared, by immunocytochemistry, the distributions of the GABA transporters GAT-1 and GAT-3 in rats, cats, monkeys and humans. We demonstrate subtle differences between the results reported in the literature and our results, such as the predominance of GAT-1 labelling in neurons rather than astrocytes in the rat cortex. We note that the optimal localisation of GAT-1 in cats, monkeys and humans requires the use of an antibody against the human sequence carboxyl terminal region of GAT-1 rather than against the slightly different rat sequence. We demonstrate that GAT-3 is localised mainly to astrocytes in hindbrain and midbrain regions of rat brains. However, in species such as cats, monkeys and humans, additional strong immunolabelling of oligodendrocytes has also been observed. We suggest that differences in GAT distribution, especially the expression of GAT-3 by oligodendrocytes in humans, must be accommodated in extrapolating rodent models of GABA homeostasis to humans.

Uniqueness criteria for continuous-time Markov chains with general transition structures

We derive necessary and sufficient conditions for the existence of bounded or summable solutions to systems of linear equations associated with Markov chains. This substantially extends a famous result of G. E. H. Reuter, which provides a convenient means of checking various uniqueness criteria for birth-death processes. Our result allows chains with much more general transition structures to be accommodated. One application is to give a new proof of an important result of M. F. Chen concerning upwardly skip-free processes. We then use our generalization of Reuter's lemma to prove new results for downwardly skip-free chains, such as the Markov branching process and several of its many generalizations. This permits us to establish uniqueness criteria for several models, including the general birth, death, and catastrophe process, extended branching processes, and asymptotic birth-death processes, the latter being neither upwardly skip-free nor downwardly skip-free.