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References Agricultural extension work has a venerable, albeit largely unrecorded, history. It is a significant social innovation, an important force in agricultural change, which has been created and recreated, adapted and developed over the centuries. Its evolution extends over nearly four thousand years, although its modem forms are largely a product of the past two centuries. Today, the organizations and personnel engaged in agricultural extension encompass a diverse range of socially sanctioned and legitimate activities which seek to enlarge and improve the abilities of farm people to adopt more appropriate and often new practices and to adjust to changing conditions and societal needs.
The term “extension” The use of the word “extension” derives from an educational development in England during the second half of the nineteenth century. Around , discussions began in the two ancient universities of Oxford and Cambridge about how they could serve the educational needs, near to their homes, of the rapidly growing populations in the industrial, urban area.
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The observed fractionation is an ancient feature related to diagenesis, burial and metamorphism. The magnitude of Sm-Nd fractionation between leachates and residues, as well as the resulting Sm-Nd ages, vary as a function of grain size and metamorphic grade. Uncleaved Welsh mudrocks of the diagenetic zone yield Sm-Nd leachate-residue ages of — Ma, in agreement with their Llanviian to Caradocian biostratigraphic ages, whereas higher grade rocks of the anchizone and epizone yield Sm-Nd ages as young as Ma.
These ages are transitional between the time of deposition and the time of regional deformation related to the Acadian Orogeny at Ma. Distinct convex-upward rare earth element REE patterns of the leachates suggest that the precipitation of early diagenetic apatite controls the trace element budget of the rock, forcing a depletion of middle REEs on the subsequently formed diagenetic phyllosilicates.
The amount of organic matter present and the extent of later prograde reactions are probable modifiers of this fractionation process. Ordovician and Devonian clastic rocks associated with the Trenton and Onondaga limestones of New York yield single-sample and multi-sample Sm-Nd isochron ages that agree well with their biostratigraphic ages of Ma and Ma, respectively.
In all cases the Sm-Nd system remained closed subsequent to the peak of diagenesis or metamorphism, including the North American rocks that show no evidence of being isotopically reset during widespread remagnetization of the subjacent limestone units in the late Paleozoic. Check if you have access through your login credentials or your institution.
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Lake Ontario bathymetric map. The action of the ice occurred along the pre-glacial Ontarian River valley which had approximately the same orientation as today’s basin. Material that was pushed southward by the ice sheet left landforms such as drumlins , kames , and moraines , both on the modern land surface and the lake bottom,  reorganizing the region’s entire drainage system. As the ice sheet retreated toward the north, it still dammed the St.
Lawrence valley outlet, so the lake surface was at a higher level. This stage is known as Lake Iroquois. When the ice finally receded from the St. Lawrence valley, the outlet was below sea level , and for a short time the lake became a bay of the Atlantic Ocean, in association with the Champlain Sea. Since the ice receded from the area last, the most rapid rebound still occurs there. This means the lake bed is gradually tilting southward, inundating the south shore and turning river valleys into bays.