This data release consists of two different datasets, waterborne resistivity profiling data and water quality data collected during profiling. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity. In June 2016, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along selected reaches of three rivers in the Delta region of Mississippi. A total of 180 kilometers (km) of continuous resistivity profiles were collected during a two-week span, with 50 km on the Quiver River, 70 km on the Sunflower River, and 60 km on the Tallahatchie River. These river reaches were selected due to groundwater and surface water continuous monitoring stations located alongside each of the streams which allowed comparison among streams and provided some information of surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For this survey a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was measured at the beginning of each profile and at the end of the last profile each day using a field conductivity meter. Data collected within each river include: Latitudelatitude, Longitudelongitude, injected current, voltage, resistance, apparent resistivity, electrode location (referenced to the position of the GPS), water depth, water temperature, water conductivity, and calculated water resistivity.

This content represents a map displaying the vector data corresponding to the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. The .sd file is an ESRI service definition file containing all the data (capatible for use in ESRI ArcDesktop). This file bundle contains 8 shapefiles, each representing an individual stream. These are all displayed in the map service definition. Users can also download the .sd file and extract the content (using 7zip, winzip, etc.) on their local machine to obtain all the stand-alone shapefiles. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This content represents a compressed folder of the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. This file bundle contains 8 .csv tables, each representing processed data for an individual stream. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This content represents a map displaying the vector data corresponding to the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. The .sd file is an ESRI service definition file containing all the data (capatible for use in ESRI ArcDesktop). This file bundle contains 8 shapefiles, each representing an individual stream. These are all displayed in the map service definition. Users can also download the .sd file and extract the content (using 7zip, winzip, etc.) on their local machine to obtain all the stand-alone shapefiles. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This content represents a compressed folder of the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. This file bundle contains 8 .csv tables, each representing raw data for an individual stream. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This content represents a compressed folder of the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. This file bundle contains 8 .csv tables, each representing raw data for an individual stream. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This content represents a compressed folder of the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. This file bundle contains 8 .csv tables, each representing raw data for an individual stream. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This content represents a compressed folder of the processed datasets for the waterborne resistivity profiling surveys of streams in the Mississippi Alluvial Plain. This file bundle contains 8 .csv tables, each representing processed data for an individual stream. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2017, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 879 kilometers (km) of continuous resistivity profiles were collected during several field excursions in 2017. Individual lengths of surveyed profiles per river include; 203 km on the Yazoo River, 197 km on the Floodway near Kennett, Missouri, 165 km on the Sunflower River, 97 km on the Black River, 83 km on the Bogue Phalia, 55 km on the Tallahatchie River, 42 km on the St. Francis River, and 37 km on the Yalobusha River. These river reaches were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Resistivity profiling was done using a ten-channel, direct-current resistivity meter and a floating, multi-electrode cable with 13 electrodes spaced 5 meters (m) apart. Resistivity measurements are made by transmitting a known current through two electrodes (transmitter) and measuring the voltage potential across two other electrodes (receiver). The multiple channels on the resistivity meter allows for voltage measurements to be made at 10 receivers simultaneously following a current injection. The configuration of the transmitter relative to the receiver(s) is referred to as an array. For these surveys, a reciprocal Schlumberger array was used, which positions the transmitting pair of electrodes toward the center of the array and the receiving pairs radiating away from the transmitter. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous, isotropic subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. The resistivity meter used an external global positioning system (GPS) and echosounder to determine the spatial location of the array and the thickness of the water column. The resistivity of the water in the river was continuously measured every 30 seconds using a field conductivity meter which included a GPS location for each measurement. Data collected within each river include: Latitude, longitude, altitude of the water surface, water depth, water resistivity, injected current, voltage, resistance, apparent resistivity, and electrode location (referenced to the position of the GPS). Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p.

This data release has three components for each of the eight surveys that were conducted in 2018: 1) a geospatial dataset of the processed data; 2) tabular data of the processed waterborne resistivity profiling data and associated water-quality data; 3) tabular data of the raw waterborne resistivity data and associated water-quality data. In addition to the newly collected data from 2018, the waterborne resistivity data from 2016 (Miller and others, 2016) is included and has been re-processed to be consistent with the processing steps currently utilized and described herein. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2018, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 906 kilometers (km) of continuous resistivity profiles were collected on 4 major streams and 4 reservoirs/lakes during several field excursions in 2018. Individual lengths of surveyed profiles per river include; 445 km on the White River, 225 km on the Black River, 76 km on the Cache, and 23 km on the Quiver River. Additionally, length of surveyed profiles on the reservoirs and lakes include; 64 km on Eutah Bend, 41 km on Roebuck Lake, 19 km on a United States Department of Agriculture On-Farm Storage Reservoir (USDA_OFS), and 13 km on Sky Lake. These river reaches and lakes were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Stream reaches surveyed in 2016, which are included as part of this data release include; 50 km on the Quiver River, 70 km on the Sunflower River, and 61 km on the Tallahatchie River. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. Methodology relating to field data collection and data processing can be found in Miller and others (2018). Data collected during each survey include: Latitude, longitude, elevation of the water surface, water depth, water resistivity, injected current, voltage, measured apparent resistivity, and electrode location (referenced to the position of the GPS receiver). References: Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p, https://doi.org/10.3133/wsp2414. Miller, B.V., Wallace, D.S., and Kress, W.H., 2016, Water-borne continuous resistivity profiling data from select streams of the Mississippi Alluvial Plain in northwestern Mississippi: U.S. Geological Survey data release, https://doi.org/10.5066/F7FT8J68. Miller, B.V., Adams, R.F., Stocks, S.J., Wilson, J.L., Smith, D.C., and Kress, W.H., 2018, Waterborne resistivity surveys for streams in the Mississippi Alluvial Plain, 2017: U.S. Geological Survey data release, https://doi.org/10.5066/F71J98ZQ.

This data release has three components for each of the eight surveys that were conducted in 2018: 1) a geospatial dataset of the processed data; 2) tabular data of the processed waterborne resistivity profiling data and associated water-quality data; 3) tabular data of the raw waterborne resistivity data and associated water-quality data. In addition to the newly collected data from 2018, the waterborne resistivity data from 2016 (Miller and others, 2016) is included and has been re-processed to be consistent with the processing steps currently utilized and described herein. In fresh water aquifers, the geoelectric resistivity of earth materials commonly has a positive correlation with hydraulic conductivity (Faye and Smith, 1994). Throughout 2018, continuous resistivity profiling data were collected, as a proxy for streambed hydraulic conductivity, along reaches of eight streams in the Mississippi Alluvial Plain of Mississippi, Arkansas, and Missouri. A total of 906 kilometers (km) of continuous resistivity profiles were collected on 4 major streams and 4 reservoirs/lakes during several field excursions in 2018. Individual lengths of surveyed profiles per river include; 445 km on the White River, 225 km on the Black River, 76 km on the Cache, and 23 km on the Quiver River. Additionally, length of surveyed profiles on the reservoirs and lakes include; 64 km on Eutah Bend, 41 km on Roebuck Lake, 19 km on a United States Department of Agriculture On-Farm Storage Reservoir (USDA_OFS), and 13 km on Sky Lake. These river reaches and lakes were selected to aid in calibration of a regional groundwater model, specifically with regards to surface water-groundwater interaction. Stream reaches surveyed in 2016, which are included as part of this data release include; 50 km on the Quiver River, 70 km on the Sunflower River, and 61 km on the Tallahatchie River. The electrical resistance is calculated by dividing the measured voltage by the applied current. The apparent resistivity is determined by multiplying the electrical resistance by a geometric factor. Apparent resistivity is not the true resistivity because a homogeneous subsurface is assumed. To estimate the true resistivity or the resistivity structure where the subsurface is heterogeneous and/or anisotropic, the apparent resistivity data were processed using an inverse modeling software program. Since these data have not been modeled they should only be used qualitatively. Methodology relating to field data collection and data processing can be found in Miller and others (2018). Data collected during each survey include: Latitude, longitude, elevation of the water surface, water depth, water resistivity, injected current, voltage, measured apparent resistivity, and electrode location (referenced to the position of the GPS receiver). References: Faye, R.E., and Smith, W.G., 1994, Relations of borehole resistivity to the horizontal hydraulic conductivity and dissolved-solids concentration in water of clastic coastal plain aquifers in the southeastern United States., U.S. Geological Survey Water Supply Paper 2414, 33 p, https://doi.org/10.3133/wsp2414. Miller, B.V., Wallace, D.S., and Kress, W.H., 2016, Water-borne continuous resistivity profiling data from select streams of the Mississippi Alluvial Plain in northwestern Mississippi: U.S. Geological Survey data release, https://doi.org/10.5066/F7FT8J68. Miller, B.V., Adams, R.F., Stocks, S.J., Wilson, J.L., Smith, D.C., and Kress, W.H., 2018, Waterborne resistivity surveys for streams in the Mississippi Alluvial Plain, 2017: U.S. Geological Survey data release, https://doi.org/10.5066/F71J98ZQ.