saw Caves ParkDay three simply consisted of one stop at the Warsaw Caves Park (NTS grid reference: 285 265). The Indian River runs through the park and is diverted, for a short distance, underground. A thin cover of glacially derived deposits on the bedrock allows for easier geological exploration. The riverbed is quite shallow (approximately a meter) and flat with only a thin layer of sand and debris. The geology in this area has had a considerable affect on the types of landforms produced. Sedimentary rock is more susceptible to erosion than granite rock, thus, features produced by water flow are more common. Throughout the park evidence of the limestone bedrock is visible. Small creeks run almost underground and odd-shaped rocks litter the surface. Part IV: Comparisons of Sites and Previous LiteratureThe geology of the study region is extremely complex because of the repeated glaciation of southern Ontario. The underlying Precambrian rock is part of the Grenville Orogenic Belt and is 1.3 to 1.0 Ga old. There are two subdivisions of the Grenville Province that border each other on the study area: the Central Gneiss Belt and the Central Metasedimentary Belt (Easton, 1992, p. 719). The transition between the Precambrian rock to the north and Paleozoic rock to the south is not a smooth one and observations support the existence of both. “The Dummer moraine demarcates the contact between Paleozoic strata and the underlying Precambrian shield exposed north of the Peterborough field. The drumlin field is underlain by southwestward-dipping Ordovician limestone and shale.” (Liberty, 1969, p. 788)Paleozoic rock to the south is specifically from the Simcoe group of Middle Ordovician Limestone (Coniglio et al., 1990, p.6) and was formed 500 to 425 million years ago (Otonabee Region Conservation Authority, 1983, p. 2-6). Natural resources such as soil, vegetation, mineral aggregates, and watercourses are greatly affected...
