Determining the Pressures and Temperatures of Metamorphism in the Gully Oven and East Rochester Formations in Rochester, NH AUTHOR: Joel Kneisley ADVISOR: Jo Laird The Gully Oven formation and East Â‡Â–Â‡Â”Â?Â‹Â?Â‹Â?Â‰ Â–ÂŠÂ‡ Â’Â”Â‡Â•Â•Â—Â”Â‡Â• ÂƒÂ?Â† Â–Â‡Â?Â’Â‡Â”ÂƒÂ–Â—Â”Â‡Â• Â‘Âˆ Â?Â‡Â–ÂƒÂ?Â‘Â”Â’ÂŠÂ‹Â•Â? Â‹Â? Â–ÂŠÂ‡ Â—ÂŽÂŽÂ› Â˜Â‡Â? ÂƒÂ?Â† ÂƒÂ•Â– Â‘Â…ÂŠÂ‡Â•Â–Â‡Â” Â‘Â”Â?ÂƒÂ–Â‹Â‘Â?Â• Â‹Â? Â‘Â…ÂŠÂ‡Â•Â–Â‡Â”ÇĄ Â‘Â‡ÂŽ Â?Â‡Â‹Â•ÂŽÂ‡Â› Rochester formation, located in Â†Â˜Â‹Â•Â‘Â”ÇŁ Â‘ ÂƒÂ‹Â”Â† Department of Earth Sciences, University of New Hampshire Rochester, NH, are pelitic schists created ÂŠÂ‘Â–Â‘Â?Â‹Â…Â”Â‘Â‰Â”ÂƒÂ’ÂŠÂ• Â?Â–Â”Â‘Â†Â—Â…Â–Â‹Â‘Â? Â‡Â•Â—ÂŽÂ–Â• ÂƒÂ?Â† Â‘Â?Â…ÂŽÂ—Â•Â‹Â‘Â? by high temperature metamorphism of turbidites consisting of aluminumrich, fine clay and sand deposits. Field Â‘Â…ÂƒÂ–Â‹Â‘Â? observations exhibit a high temperature contact between schist and quartzite rocks in the Gully Oven formation, and Â‹Â?Â‡Â”ÂƒÂŽ Â•Â•Â‡Â?Â„ÂŽÂƒÂ‰Â‡Â• the East Rochester formation displays folding and overturned bedding as ÂŠÂ‘Â?Â’Â•Â‘Â? Â”Â‘ÂŒÂ‡Â…Â–Â‹Â‘Â?Â• well as staurolite inclusions within the andalusite. Because estimates of conditions during metamorphism are not previously established for either formation, pressures and temperatures of metamorphism for the Gully Oven and East Rochester formations are estimated using fieldwork, petrology, and thermo-barometry. The Gully Oven formation shows an andalusite + garnet + biotite assemblage and the East Rochester formation shows an andalusite + staurolite + biotite assemblage. The Gully Oven formation assemblage is indicative of high temperature, higher grade metamorphism with temperatures in the 500 to 700-degrees Celsius range. The East Rochester formation assemblage shows intermediate/high metamorphism with temperatures ranging from 400 to 600 degrees Celsius. Both formations show low pressure metamorphism, with pressures not exceeding 300 kb. ÂŠÂ‡ Â—ÂŽÂŽÂ› Â˜Â‡Â? ÂƒÂ?Â† ÂƒÂ•Â– Â‘Â…ÂŠÂ‡Â•Â–Â‡Â” Â‘Â”Â?ÂƒÂ–Â‹Â‘Â?Â• ÂƒÂ”Â‡ Â–Â™Â‘ Â?Â‡Â–ÂƒÂ?Â‘Â”Â’ÂŠÂ‘Â•Â‡Â† Â–Â—Â”Â„Â‹Â†Â‹Â–Â‡Â• ÂŽÂ‘Â…ÂƒÂ–Â‡Â† Â‹Â? Â‘Â…ÂŠÂ‡Â•Â–Â‡Â”ÇĄ Č‹Â•Â‡Â‡ Â‹Â‰Â—Â”Â‡ ÍłČŒÇ¤ Â‡Â–Â”Â‘ÂŽÂ‘Â‰Â‹Â… ÂƒÂ?ÂƒÂŽÂ›Â•Â‹Â• Â™ÂƒÂ• Â”Â‡Â“Â—Â‹Â”Â‡Â† Â–Â‘ Â‹Â?Â–Â‡Â”Â’Â”Â‡Â– Â–ÂŠÂ‡ Â’Â”Â‡Â•Â•Â—Â”Â‡Â• ÂƒÂ?Â† Â–Â‡Â?Â’Â‡Â”ÂƒÂ–Â—Â”Â‡Â• Â‘Âˆ Â?Â‡Â–ÂƒÂ?Â‘Â”Â’ÂŠÂ‹Â•Â? Â‹Â? Â–ÂŠÂ‡Â•Â‡ Â–Â™Â‘ ÂˆÂ‘Â”Â?ÂƒÂ–Â‹Â‘Â?Â• Â–Â‘ Â—Â?Â†Â‡Â”Â•Â–ÂƒÂ?Â† Â–ÂŠÂ‡ ÂŽÂ‘Â…ÂƒÂŽ Â‰Â‡Â‘ÂŽÂ‘Â‰Â‹Â…ÂƒÂŽ ÂŠÂ‹Â•Â–Â‘Â”Â›Ç¤ Sample Tourmaline 18NHJK1 18NHJK2 18NHJK4C X 18NHJK5A X Garnet X X X X Figure 2: Twinned staurolite porphyroblast with unknown texture developing within the core of the grain. (sample 18NHJK1) Figure 3: Andalusite porphyroblast showing overgrowth of staurolite. (sample 18NHJK2) Figure 4: Compositional variation within the rock. Biotite rich zone is at the bottom and the staurolite rich zone is at the top of the photo. (sample 18NHJK5A) Figure 5: Garnet porphyroblast within a biotite zone. The dark elongate grains are titanium bearing ilmenite. (sample 18NHJK4C) Ilmenite X X X X Biotite X X X X Chlorite X X X X Muscovite X X X X Quartz X X X X Staurolite Andalusite Cordierite X X X X X X X X X Table 1: Mineral Assemblages Figure 1: Map of field area in Rochester, NH. Geology map is from GRANIT download (2017). Topographic map is from GRANIT download (1998). Index map from wiki.radioreference.com (2019). EARTH & OCEAN SCIENCE Winning Project 2019 Conclusions: â€˘ Â™Â‘ Â†Â‹Â•Â–Â‹Â?Â…Â– Â?Â‹Â?Â‡Â”ÂƒÂŽ Â‰Â”Â‘Â™Â–ÂŠ Â‡Â˜Â‡Â?Â–Â• Â‘Â…Â…Â—Â”Â”Â‡Â† Â‹Â? Â–ÂŠÂ‡ ÂƒÂ•Â– Â‘Â…ÂŠÂ‡Â•Â–Â‡Â” Â‘Â”Â?ÂƒÂ–Â‹Â‘Â?Ç¤ â€˘ Â—ÂŽÂŽÂ› Â˜Â‡Â? 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In 2013, Cesium (Cs) contamination from the Fukushima-Daiichi Nuclear Power Plant destabilization was observed south of the KE at ~165E and >500m depth on the 26.5 sigma-theta density surface. It is well established that at the surface, strong currents such as the KE behave as barriers to water transport, but to what longitude and depth these barriers extend is still being disputed. Using highresolution model velocity fields, water parcel trajectories are integrated back in time on the 26.5 surface from the date and location of observation to the date of the maximum Cs input to the ocean. Using those trajectories most likely to carry Cs, i.e. those that interacted with the mixed layer in the region of maximum contamination, we developed a map of the most probable path and timeline to the observed deep Cs location. This map suggests that the KE acted as a permeable transport barrier to 26.5 waters out to ~165E. More generally, an additional forward in time trajectory simulation from the regions where the Cs most likely entered the 26.5 waters to the date of observation suggests that the KE impeded southward transport of Cs at all locations west of ~157E. 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