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Thesis advisor: Owen Stanwood / Making Nations: The Northeastern Borderlands in an Age of Revolution, 1760-1820 examines migration within northeastern North America, and the gradual formation of a meaningful border between the District of Maine and the Province of New Brunswick. The American Revolution, though it divided the northeast between New England and British North America, did not fundamentally change attitudes toward the borderland. For decades, the region had been a special sort of frontier – a more connected frontier, offering migrants from southern New England better access to Atlantic trade. The post-revolutionary era rapidly reverted to pre-war patterns, as settlers crossed a largely meaningless border looking for fertile land and economic connectivity. These settlers, I argue, were not late loyalists, choosing British territory, or early republicans, choosing the U.S. This was one migration, to the borderland and the similar opportunities on both sides. So how did migration within a shared borderland become immigration across a meaningful border? Post-revolution, both Congregationalists and Catholics began to build networks in Maine that stopped at the border. A Congregational missionary society, the Society for Propagating the Gospel Among the Indians and Others in North America, realized it could secure state funding from Massachusetts by advertising itself as a tool for managing the growing settlements in Maine. State money helped the society grow rapidly, and as similar groups formed they chose to join the pioneer society as partners rather than compete with it. Meanwhile, Congregational women created institutions called “ladies cent societies,” which provided a massive infusion of funding into the system. The resulting Congregational network grew to encompass almost the entire American half of the borderland. At the same time, a Catholic network also grew in Maine, connecting the Catholic Passamaquoddy and Penobscot people to Boston, as well as to Irish Catholics along Maine’s coast. As these networks grew they changed eastern Maine from a place that was attractive because of its connections with British North America, to a place that was attractive because of its connections with New England. These networks made the border meaningful – and immovable. Though politicians on both sides persisted for years in believing they could still adjust the border, they were wrong. It had already taken root. / Thesis (PhD) — Boston College, 2019. / Submitted to: Boston College. Graduate School of Arts and Sciences. / Discipline: History.

Thesis advisor: Noah P. Snyder / The Sheepscot River watershed is 590 km2 located in mid-coast Maine. Two branches comprise the river: the main stem and the West Branch, which merge in North Whitefield before flowing into the Gulf of Maine. The Sheepscot River has an imposed form that is strongly influenced by the Norumberga Fault Zone and it flows through glacial deposits. The watershed has a temperate climate because of its location in mid-latitudes in the northern hemisphere. Water temperatures vary in the Sheepscot River over time and along the length of the river. The temporal and spatial variability of the river is due to air temperature, precipitation, discharge from the Palermo Fish Rearing Station, Long Pond, tree shade, confluence, and drainage area. Analysis of these hypothesized controls revolves around field water temperature measurements made between August 2005 and January 2006 and data collected from the North Whitefield gauging station. Supplementary digital spatial data from the Maine Geographic Information Systems data set were also used. Field measurements were taken at seven sites directly upstream and downstream of assumed controls. Climactic features of the watershed exert the main control over the entire river. Air temperature is the first order controls on water temperatures. Precipitation has some effect on water temperature but of less significance than air temperature. The river system has three areas that are affected by different combinations of the other controls: the upper main stem, the West Branch, and the lower main stem. Discharge from the Palermo Fish Rearing Station is the second major controlling factor of water temperature in the upper main stem. Its buffering effect is diluted downstream. Long Pond also affects the upper main stem by warming the water in the summer and cooling it in the winter. Drainage area explains variability in the West Branch and lower main stem. As drainage area increases downstream, water temperatures are controlled by more integrated factors. As a result of this the West Branch fluctuates more than the main stem because it has a smaller drainage area. Temperatures in the downstream reaches are less sensitive to any single control. Confluence and tree cover exert less influence over the system than other controls. / Thesis (BS) — Boston College, 2006. / Submitted to: Boston College. College of Arts and Sciences. / Discipline: Geology and Geophysics. / Discipline: College Honors Program.

Seismic refraction data collected in 1985 by the USGS were used in this study to derive the P and S velocity structure of the crust beneath the Gulf of Maine. The data quality differs among instruments and is affected by surficial lateral heterogeneities, a ringy source signature and reverberations. Velocity models of the crust were computed by one-dimensional raytracing and by wavefield continuation. Pg arrivals were modeled using both techniques to derive the P velocity of the upper 5-15 km of the crust and give very similar results. Strong Sg arrivals were also observed, and computed S amplitudes generated from P-S conversion for different scenarios show that the observed S wave is generated at the basement top. Two small sediment basins are indicated in the Central Plutonic Zone and two faults are suggested in the Fault Zone and the Central Plutonic Zone, respectively. Beneath the sediments the layering is uniform with dips of less than 2° and a fairly laterally homogeneous velocity structure, in spite of lateral variations in reflectivity. P and S velocities increase from 5.3 and 2.8 km/s, respectively, at the basement to 6.4 and 3.7 km/s at 10 km depth. A laterally discontinuous low velocity zone is indicated at 6-10 km depth which might be caused by laccolithic granitic intrusions. However, magnetic and gravity data do not show indications for felsic intrusions where the low velocity zones are observed. Velocity differences among some instruments suggest anisotropy in the upper 6 km of the crust, as observed in onshore Maine. These instruments indicate velocities parallel to the structural grain of the Appalachians of 6.1-6.4 km/s and velocities transverse to the grain of 5.8-6.1 km/s in the depth range 2-6 km. Cashes Ledge granite, a site of an intense magnetic high, has a reduced velocity compared to surrounding rocks and might extend to at least 10 km depth. Poisson's ratio for the upper crust ranges from 0.23-0.26. To derive the velocity structure of the middle and lower crust, wide-angle reflections interpreted to be PmP and SmS were modeled by one-dimensional raytracing. In addition synthetic seismograms were computed using the WKBJ method to constrain possible middle and lower crust velocity models by their PmP and SmS amplitudes. Recorded PmP and SmS wide-angle reflections have quite different amplitudes and travel-times among instruments suggesting a heterogeneous lower crust. The crust below 10 km depth has an average P velocity of 6.5-6.8 km/s and an average S velocity of 3.7-3.9 km/s. Most instruments indicate a Poisson's ratio of around 0.25 between 10 km depth and Moho and one instrument suggests a Poisson's ratio of 0.28. Hence, the middle and/or lower crust under the Gulf of Maine is heterogeneous and represents average crust modified by mafic intrusions, probably during Mesozoic extension. Moho depth is indicated between 30 and 37 km depth. Wide-angle reflections coming from 28 km depth as indicated by two instruments are interpreted to come from the top of a lower crustal intrusion. This interpretation is supported by an observed mismatch between the models giving a thickness of 28 km and the reflection data. Although it represents a different geological terrane, the velocity and thickness of the crust beneath the central Gulf of Maine is very similar that onshore Maine. / Graduation date: 1991