[1] Nitrogen transport and groundwater-surface water interactions were examined in a coastal plain watershed in the southeastern United States. Groundwater age dates, calculated using chlorofluorocarbon and tritium concentrations, along with concentrations of nitrogen species and other redox-active constituents, were used to evaluate the fate and transport of nitrate. Nitrate is stable only in recently recharged (<10 years) water found in the upper few meters of saturated thickness in the upland portion of a surficial aquifer. Groundwater with a residence time between 10 and 30 years typically has low nitrate and elevated excess N 2 concentrations, indications that denitrification has reduced nitrate concentrations. Groundwater older than 30 years also has low nitrate concentrations but contains little or no excess N 2 , suggesting that this water did not contain elevated concentrations of nitrate along its flow path. Nitrate transport to streams varies between first-and third-order streams. Hydrologic, lithologic, and chemical data suggest that the surficial aquifer is the dominant source of flow and nitrate to a first-order stream. Iron-reducing conditions occur in groundwater samples from the bed and banks of the first-order stream, suggesting that direct groundwater discharge is denitrified prior to entering the stream. However, nitrogen from the surficial aquifer is transported directly to the stream via a tile drain that bypasses these reduced zones. In the alluvial valley of a third-order stream the erosion of a confining layer creates a much thicker unconfined alluvial aquifer with larger zones of nitrate stability. Age dating and chemical information (SiO 2 , Na/K ratios) suggest that water in the alluvial aquifer is derived from short flow paths through the riparian zone and/or from adjacent streams during high-discharge periods.

Effects of cultural eutrophication with respect to phosphorus enrichment in coastal plain streams of the Neuse River basin are much greater than for nitrogen. The eutrophication loading index of phosphorus ranged between 2 and 12 times, and values typically were 5 to 6 times the estimated background yield for second-and higher-order streams. The eutrophication loading index of total nitrogen ranged between 1 and 5 times, and values typically were about 2 times the estimated background yield.

Cost‐effective monitoring strategies exist for estimating mean depth to the water table and for characterizing fluctuations about that mean. These strategies can also be used to evaluate the utility of sparse water level data sets for making such estimates. This type of information is needed to design or reduce costs of observation well networks, to characterize regional water‐table fluctuations for use in maps or models, and to calibrate ground‐water models using hydraulic head estimates. The study is based on a statistical analysis of hourly water levels measured at observation wells by the U. S. Geological Survey (USGS) over a five‐year period. Using Monte Carlo simulation techniques, sampling results for different monitoring strategies were compared with parameters of the underlying distribution of hourly water levels. Monthly, bimonthly, quarterly, and even tri annual water‐level monitoring was found to effectively estimate mean water table depth and standard deviation to within 30 cm. Quarterly and tri annual sampling were found more cost‐effective than monthly observations, and electronic monitoring more effective than manual measurements for sampling made more frequently than monthly. Results have broad application for studies involving surficial aquifers in humid regions of the world where annual rainfall exceeds 50 cm and is reasonably distributed throughout the year. Governmental agencies and universities have a wealth of water table monitoring records, collected either through ambient monitoring or as part of a permit requirement or study. These sparse data sets hold the promise of significantly increasing the hydro geologic knowledge of water table behavior in many regions of the world.