Kansas Geological Survey, Bulletin 188, originally published in 1968
Prepared by the United States Geological Survey and the State Geological Survey of Kansas, with the cooperation of the Environmental Health Services of the Kansas State Department of Health and the Division of Water Resources of the Kansas State Board of Agriculture.
Originally published in 1966 as Kansas Geological Survey Bulletin 188. This is, in general, the original text as published. The information has not been updated. An Acrobat PDF version (10 MB) is also available; plates available separately.
Both surface and ground water are used for irrigation in parts of Cloud, Jewell, and Republic counties in north-central Kansas. The combination of surface-water irrigation and recharge from precipitation has caused some high ground-water levels in some of the upland areas.
In the lowland areas, alluvial deposits yield as much as 1,400 gallons a minute to wells, and about 12,300 acre-feet of ground water is pumped annually for irrigation and other uses. It is estimated that 710 acre-feet of this quantity was removed from the Republican River in 1963 by the pumping of ground water. Coefficients of transmissibility from 61 well sites were used in making the above estimate.
Ground-water recharge from precipitation in the area was estimated to be 0.6 inch and ground-water losses to evapotranspiration to be less than 0.2 inch.
Chlorides in ground water in northern Cloud County are tabulated and the areas mapped where the ground water might be unfit for use in irrigation.
Irrigation of the upland areas in northeastern Jewell and western Republic counties began in 1958 with use of surface water from the Harlan County Reservoir in Nebraska and the Lovewell Reservoir in Kansas. Water levels in these areas were shallow prior to irrigation, and because the lateral permeability of the water-bearing material was low, it was expected that seepage from canals and applications of surface water probably would cause temporary detrimentally high water levels. It was necessary to collect data concerning water levels so that areas of present high water levels or potential high water levels could be delineated.
The flow of the Republican River is regulated so that there will be adequate water available for municipal sewage disposal and for navigation. Therefore, information concerning the effects on the flow of the River caused by pumping of ground water from the alluvial deposits in the river valley was needed. In some areas of northern Cloud County ground water in the alluvial deposits is highly mineralized. Information was needed regarding the chloride content of the ground water, the areal extent of the chlorides, and the change of chloride with time, if any, in water from wells.
The Republican River area is included in the northern 8 miles of Cloud County, parts of the western 3 ranges of Republic County, and the northeastern part of Jewell County (Fig. 1). The area is part of the "Lower Republican River Unit" as defined by the Kansas Water Resources Board (June, 1961). The lowland area is outlined by the heavy dashed line on Plate 2.
Figure 1--Location of area described in this report, and other areas for which ground-water reports have been published by the State Geological Survey of Kansas or are in preparation.
The principal topographic features that are pertinent to the ground water of the area are: the high flat upland plains, similar to those in western Kansas; the gently rolling areas developed on the Dakota Formation; the broad, flat valley of the Republican River; the narrower valleys of Buffalo and White Rock creeks; the broad, flat terraces in the valleys; the deeply dissected area between the uplands and the river valleys; and the salt marshes in northern Cloud County.
There are 1,140 square miles drained by the Republican River between the gages at Hardy, Nebraska, and Concordia, Kansas (Pl. 2). Of this area, 342 square miles is above the gage at Loveland on White Rock Creek, and 330 square miles is above the gage at Jamestown on Buffalo Creek. The remainder of the area is drained by minor streams tributary to the Republican River.
[Note: The nomenclature and classification of the geologic units described in the report follow the usage of the State Geological Survey of Kansas and differ somewhat from usage adopted by the U.S. Geological Survey.]
Detailed descriptions of the geology of the Republican River area are given by Fishel (1948), Fishel and Leonard (1955), and Bayne and Walters (1959) in reports on the geology and ground-water resources of Republic, Jewell, and Cloud counties, respectively. Because this investigation does not include a detailed study of the geology, only a brief summary is given. The reader is referred to the Selected References for more detailed geologic and hydrologic information.
The rocks that crop out in the area are sedimentary and range in age from Cretaceous to Recent. A generalized geologic section is given in Table 1. Three geologic sections showing the relationship of the water-bearing materials are shown on Plate 3. Two diagrammatic sections (Fig. 14) showing the relationship of the brackish water to the alluvial deposits are discussed in the section on Chlorides in Ground Water.
Table 1--Generalized geologic section in the Republican River area (modified after Fishel, 1948; Fishel and Leonard, 1955; Bayne and Walters, 1959; Jewett, 1959; and Franks, 1966).
System | Series | Stage | Stratigraphic unit |
Maximum thickness, ft |
Physical character | Remarks | |
---|---|---|---|---|---|---|---|
Quaternary | Pleistocene | Recent | Alluvium | 130 | Clay, silt, sand, and gravel, unconsolidated | Yields up to 1,400 gpm of water | |
Wisconsinan | Terrace deposits | 125 | Clay, silt, sand, and gravel, stream deposited; coarser materials generally in lower part of deposits | Yields large quantities of water | |||
Wisconsinan and Illinoisan |
Eolian silts | 20 | Silt, mantling upland and older terrace deposits along major streams | Yields no water, but some observation wells screened in this unit | |||
Illinoisan | Loveland and Crete formations, undifferentiated |
75 | Silt and clay, waterlaid, containing minor amounts of sand and gravel; generally more gravel near base | Yields small to moderate quantities of water | |||
Crete Formation | 30 | Sand, gravel, and silt in terrace position along some major streams. Gravel is principally limestone | Lies generally above water table, but yields small quantities of water where below water table | ||||
Kansan | Sappa Formation | 60 | Sand and gravel, locally derived, overlain by silt and clay. Occurs in deeper parts of Republican River valley | Yields large quantities of water to wells in northern Republic County; water has high chloride content in part of Cloud County | |||
Grand Island Formation | |||||||
Cretaceous | Upper Cretaceous |
Carlile Shale |
Blue Hill Shale Member |
200 | Fissile, noncalcareous, gray to black, marine shale; contains thin sandy zone at top and septarian and discoidal concretions | Yields little or no water, but some observation wells screened in this unit | |
Fairport Chalk Member |
100 | Shale, thin-bedded, calcareous | Yields little or no water to wells | ||||
Greenhorn Limestone | 90 | Limestones and shales, thin-bedded, chalky; thin streaks of bentonite | Yields small quantities of hard water, but some observation walls screened in this unit | ||||
Graneros Shale | 40 | Clay and fissile shale, noncalcareous, black and olive drab | Yields small quantities of hard water, but some observation walls screened in this unit | ||||
--?-- | Dakota Formation | 300 | Clay, shale, siltstone, and sandstone; some lignite | Yields moderate to large quantities of water. High chloride content locally and in lower deposits | |||
Lower Cretaceous |
The author spent 3 months in the fall of 1962 and 4 months during the summer of 1963 gathering hydrologic data in the field and several months during the winters 1962-64 analyzing both field and published data. Beginning in 1956 the U.S. Bureau of Reclamation measured water levels in about 360 observation wells. These data and data collected by the author were used to prepare hydrographs and water-level maps.
Information concerning the depth, depth to water, diameter, screen and yield was collected for 101 irrigation wells in Cloud County and 86 wells in Republic County. This information, together with geologic information obtained from 25 test holes, 320 well logs furnished by the U.S. Bureau of Reclamation, and previously published information, was used to prepare the map of saturated-thickness of unconsolidated deposits. Three geologic cross sections were prepared using the same data to show the relationship of the geology to the hydrology of the area.
It is planned that a separate report containing the basic data of the area on which this summary report is based will be prepared and will contain the tables of well data and logs of wells and test holes. Table 3 of this report will be updated and new information will be included. This report of basic data will be available to interested readers, for a reasonable fee, upon request from the State Geological Survey of Kansas, Lawrence, Kansas.
Coefficients of transmissibility were computed or estimated from data at 61 well sites. Three detailed aquifer tests using one to four observation wells, 22 step-drawdown (single well) tests, and one single well-recovery test were used at 26 sites. At the remaining 35 sites, estimates were made from specific capacities reported by the owners.
Water samples collected prior to 1960 were analyzed for several constituents by chemists in the Sanitary Engineering Laboratory of the Kansas State Department of Health under the supervision of H. A. Stoltenberg. Samples collected after 1960 were analyzed in the field for chlorides only. The analyses of the samples collected prior to 1960 are published in Kansas Geological Survey bulletins 73, 139, and 155, and those collected after 1960 are given in this report.
The altitudes of measuring points of wells and test holes were determined by the U.S. Bureau of Reclamation and by the Kansas District Office of the U.S. Geological Survey and the State Geological Survey of Kansas.
The locations of wells and test holes in this report (Fig. 2) are designated according to the General Land Office Surveys in the following order: township, range, section, quarter section, quarter-quarter section, and quarter-quarterquarter section (lO-acre tract). The quarter sections, quarter-quarter sections, and quarter-quarter-quarter sections are designated a, b, c, or d in counterclockwise direction beginning in the northeast quarter section.
Figure 2--Well-numbering system used in this report. The well is in SE SE NE sec. 26, T 2 S, R 5 W.
If more than one well or test hole is located in the same l O-acre tract, the location letters are followed by a serial number.
The locations of these wells and test holes and the locations of the surface-water gaging stations are shown on Plate 3.
The annual precipitation at Concordia, Belleville, and Burr Oak is shown in Figure 3. The normal monthly precipitation at Concordia is shown in Figure 4.
Figure 3--Annual precipitation at Concordia, Belleville, and Burr Oak. (Data from U.S. Weather Bureau.)
Figure 4--Normal monthly precipitation at Concordia, Kansas, for the period 1931-61. (Data from U.S. Weather Bureau.)
The quantity of water that an aquifer will yield to wells depends upon the hydrologic properties of the materials in the aquifer. The ability of an aquifer to transmit water is measured by its coefficient of transmissibility. The coefficient of transmissibility (T) of an aquifer is defined as the number of gallons of water that will move in 1 day through a vertical strip of aquifer 1 foot wide and the full thickness of the aquifer, under a hydraulic gradient of 100 percent or 1 foot per foot, at the prevailing temperature of the water. The coefficient of permeability (P) is expressed as the rate of flow, in gallons per day, through a cross-sectional area of 1 square foot under a hydraulic gradient of 1 foot per foot. The coefficient of permeability can be computed by dividing the coefficient of transmissibility by the thickness (m) of the aquifer. The coefficient of storage (S) of an aquifer is defined as the volume of water it releases or takes into storage per unit surface area of the aquifer per unit change in the component of head normal to that surface. Under water-table conditions the coefficient of storage is practically equal to the specific yield, which is defined as the ratio of volume of water a saturated material will yield to gravity in proportion to its own volume.
The step-drawdown tests were analyzed by the following Theis (1935) equation:
where Q = discharge of pumped well, in gpm;
s = drawdown, in feet (corrected for well loss);
T = coefficient of transmissibility, in gallons a day per foot;
S = coefficient of storage;
rw = radius of well, in feet;
t = time, in days after pumping started.
The results of the tests are given in Table 2.
Table 2--Results of pumping tests in the Republican River area, Kansas.
Well number |
Geologic source* |
Coefficient of transmissibility, in gpd/ft |
Coefficient of permeability, in gpd/ft2 |
Type of test† |
---|---|---|---|---|
Republic County | ||||
1-3W-3bc | Qd | 320,000 | 4,000 | SC |
1-3W-5aa | Qd | 190,000 | 4,200 | SC |
1-4W-17ab | Qd | 288,000 | 5,500 | SC |
1-5W-18ab | Qd | 50,000 | 1,500 | SC |
2-4W-31bc | Qd | 60,000 | 2,200 | SC |
3-4W-8ccb | Qa | 100,000 | 2,500 | OW |
3-4W-17bd | Qa | 72,000 | 2,400 | SC |
3-4W-17db | Qa | 45,000 | 1,000 | SC |
3-4W-20aa | Qa | 60,000 | 1,500 | SC |
3-4W-32da | Qa | 110,000 | 2,700 | SC |
4-4W-4bc | Qa | 50,000 | 1,560 | SC |
4-4W-4db | Qw | 175,000 | 4,260 | SDD |
4-4W-4dc2 | Qw | 130,000 | 3,000 | OW |
4-4W-8ad | Qa | 75,000 | 1,500 | SC |
4-4W-8db | Qa | 65,000 | 2,200 | SC |
4-4W-8dd | Qa | 75,000 | 1,700 | SC |
4-4W-9ab | Qw | 125,000 | 2,500 | SC |
4-4W-9ca | Qa | 150,000 | 3,750 | SC |
4-4W-15cd2 | Qi | 10,000 | SC | |
4-4W-17da | Qa | 200,000 | 4,000 | SC |
4-4W-17dd | Qa | 90,000 | 1,800 | SC |
4-4W-21caa | Qw | 170,000 | 3,600 | SDD |
4-4W-21cab | Qw | 120,000 | 3,000 | SDD |
4-4W-22ca | Qi | 60,000 | 2,200 | SC |
4-4W-22cc | Qi | 95,000 | 2,500 | SC |
4-4W-27ddc | Qw | 70,000 | 2,000 | SDD |
4-4W-29db | Qa | 80,000 | 2,000 | SC |
4-4W-33aa | Qw | 140,000 | 3,500 | SC |
4-4W-34baa | Qw | 120,000 | 3,200 | SC |
Cloud County | ||||
5-1W-21cd | Qw | 60,000 | 1,500 | SC |
5-1W-30aac | Qa | 160,000 | 4,000 | SC |
5-1W-31bd | Qw | 185,000 | 3,400 | SC |
5-1W-32bc | Qw | 80,000 | 1,600 | SDD |
5-2W-19bc | Qw | 62,000 | SC | |
5-2W-21ad | Qa | 110,000 | 2,750 | SC |
5-2W-21dd | Qa, Qk | 40,000 | 800 | SDD |
5-2W-25cb | Qw | 100,000 | 2,000 | SC |
5-2W-25cc | Qw | 270,000 | 5,700 | OW |
5-2W-31cc | Qd | 20,000 | 1,000 | SC |
5-2W-32cb | Qw | 100,000 | 3,200 | SDD |
5-2W-32db | Qw | 190,000 | 6,300 | SDD |
5-2W-34aab | Qw | 140,000 | 2,400 | SDD |
5-2W-36ab | Qw | 300,000 | 6,300 | SC |
5-2W-36bc | Qw | 30,000 | 1,800 | SC |
5-3W-21ca | Qa | 150,000 | 4,000 | SDD |
5-3W-22bc1 | Qw | 280,000 | 3,700 | R |
5-3W-35abc | Qa | 130,000 | 2,600 | SDD |
5-3W-36bb | Qa | 190,000 | 3,400 | SDD |
5-4W-3abd | Qw | 130,000 | 3,200 | SC |
5-4W-3dd | Qw | 90,000 | 2,600 | SDD |
5-4W-8dad | Qw | 100,000 | 2,600 | SC |
5-4W-9cca | Qw | 330,000 | 5,000 | SDD |
5-4W-13dad | Qw | 140,000 | 4,800 | SDD |
5-4W-15da | Qa | 260,000 | 4,300 | SDD |
5-4W-16dd | Qw | 93,000 | 2,300 | SDD |
5-4W-17aa | Qw | 160,000 | 3,800 | SDD |
5-4W-21ba | Qw | 93,000 | 2,200 | SDD |
5-4W-22ab | Qw | 125,000 | 2,400 | SC |
6-1W-2ca | Qw,Kd | 50,000 | 1,700 | SDD |
6-1W-4bc2 | Qw | 55,000 | 1,400 | SDD |
6-1W-12ab | Qw | 190,000 | 5,100 | SDD |
* Qd, Pleistocene deposits, undifferentiated;
Qa, Recent alluvium;
Qw, Wisconsinan terrace deposits;
Qi, Illinoisan terrace deposits;
Qk, Kansan deposits;
Kd, Dakota Formation. † SC, specific capacity; OW, observation wells; SDD, step drawdown; R, recovery. |
Water levels in the area are shown by hydrographs (Fig. 5-10), by water-level contours (Pl. 2 and 3), and by the depth to water (Pl. 1). The areas of zero water level (corresponding closely to areas of waterlogging) are shown by blue lines on Plate 1 for part of the area.
Water levels in wells fluctuate in response to additions to or withdrawals from the aquifers. In general, the hydrographs show a downward trend of water levels for the period of deficient precipitation, 1953-56 (Fig. 3), and the rise after 1956 is owing to an increase in precipitation. After 1958 irrigation from surface sources has contributed to the rise in water level in some areas.
In the upland areas of western Republic and eastern Jewell counties, water levels rise during the summer months (see Fig. 5, 6, and 7) and fall during the winter months. In addition to the higher normal monthly precipitation in May and June (Fig. 4), water is applied for irrigation starting in Mayor June. Thus, a rise of groundwater levels would be expected during the summer months along with some detrimentally high ground-water levels in areas of normal shallowwater levels (Pl. 1, 2, 3).
Figure 5--Hydrographs of wells in the undifferentiated Pleistocene aquifers of Jewell County, Kansas.
Figure 6--Hydrographs of wells in undifferentiated Pleistocene aquifers (3-5W-25aa). and Cretaceous (Greenhorn) aquifers (3-5W-25aa; 3-5W-22cc; and 4-5W-15dd) of upland Republic County, Kansas.
Figure 7--Hydrographs of wells in Cretaceous (Greenhorn Limestone) aquifers of upland Republic County, Kansas.
In the lowland areas, water levels are generally related to the local recharge from precipitation and the discharge rate of the Republican River (Fig. 8, 9, and 10). Where pumping of ground water occurs, the water level is lowered during the dry summer months. Evapotranspiration also tends to lower the water levels in the lowland area.
Figure 8--Hydrographs of wells in the Pleistocene aquifers and monthly flow in the Republican River near Hardy, Nebraska. (Qd, undifferentiated Pleistocene deposits; Qa, Recent alluvium.)
Figure 9--Hydrographs of wells in the alluvial aquifers (Recent) and monthly flow in the Republican River at Scandia, Kansas.
Figure 10--Hydrograph of well in Recent alluvial aquifer and monthly flow in the Republican River at Concordia, Kansas.
In 1963, the alluvial deposits, excepting those of Kansan age, along the lowland area of the Republican River (Pl. 4) contained about 580,000 acre-feet of water. This estimate is based on the volume of saturated material above the Kansan deposits (which is generally a poor aquifer and contains brackish water in northern Cloud County) and an assumed coefficient of storage of 0.2. However, not all of this water in storage is available for irrigation use, and should the water levels decline, the yields of the wells will decline, and a time may be reached when yields will no longer be adequate for irrigation, but yields will continue to be adequate for stock, domestic, or other uses. Because of the dissection of the upland areas, no attempt was made to compute the ground water in storage in the upland.
The recharge to the ground-water reservoir is by direct infiltration from precipitation in the area, by seepage from streams and ponds, and by seepage from surface-water irrigation. Most of the precipitation falling on the eroded upland areas runs off, returns to the atmosphere by evapotranspiration either locally from soil moisture or after reaching the water table and moving laterally to the confluence of the water table and the upland streams and drains, or by seeping downward into the Cretaceous aquifers where it moves laterally to the streams or drains. As evapotranspiration is less in the winter than the summer months, small amounts of this discharge should reach the streams to be gaged but might be delayed for as long as 6 months. When precipitation is above normal on the non-irrigated areas of the uplands, recharge is increased and a rise in water level is expected together with a slight increase of evapotranspiration and a slight increase in the lateral flow to streams. When precipitation is below normal the discharge to evapotranspiration and streams is more than the recharge and a decline of water levels results. After 1958, irrigation using surface water has resulted in additional recharge in the irrigated areas of northwestern Republic County and the adjacent areas of Jewell County (Fig. 5-7).
Ground water in the lowlands is recharged by local precipitation along the valley bottoms and terraces, by lateral flow from the Republican River, by seepage from the shales, sandstones, and limestones along the valley walls, and in the Hardy to Scandia area by irrigation with surface water. The discharge from the lowland areas is by evapotranspiration, by pumpage of ground water for irrigation, municipal, domestic, and stock uses, and by seepage to some reaches of the streams.
The recharge to the aquifers along the Republican River can be estimated if it is assumed that base flow in the river is from ground water and that base flow (Q80) is about 80 percent time on the flow-duration curves. Prom the curves (Furness, 1959) the Q80 at Hardy is 202 cfs (cubic feet per second) and at Concordia 235 cfs. If this base flow is assumed to be equal to recharge over the area of 1,140 square miles between the gages, the recharge would be about 0.4 inch per year. Because trees and other vegetation along the streams obtain part of their water supply from ground water, the recharge must be greater than 0.4 inch to supply both the streams and vegetation.
The recharge can also be estimated from the Base Flow Data (Busby and Armentrout, 1965). The recharge to the area would be the base flow in the streams draining the area. During the growing season, the water lost to evapotranspiration along the valley walls and streams would not reach the gage to be measured; therefore, recharge in the area would be larger than gaged on the stream. The maximum recharge to the area would approach the base flow during the non-growing season, but as factors other than evapotranspiration are involved, the recharge is between the base flow in the streams during the growing season and during the non-growing season. In this report the mean of record for the year (from Base Flow Data) was used to estimate the recharge.
The mean of record base flow for the year (Busby and Armentrout, 1965) for White Rock Creek at Lovewell, Kansas, was 7.1 0 cfs for an area of 342 square miles or 0.30 inch. In the Little Blue River near Endicott, Nebraska, the basin immediately northeast of the area, the base flow was 157 cfs for an area of 2,340 square miles or 0.84 inch. In the Solomon River, south of the area, the difference in base flow between Beloit and Niles, Kansas, was 61 cfs for an area of 1,240 square miles or 0.62 inch. The average of these was 0.59 inch and includes some loss to evapotranspiration.
An examination of the aerial photographs for the area indicated that there were about 6 square miles of cottonwood and willow trees along the valley bottom of the Republican River. About 4 square miles were between the Hardy and Concordia gages and 2 square miles between Concordia and the Clay county line. According to Blaney (1957, p. 129), the evapotranspiration rate for cottonwood trees in California was 1.15 times the pan evaporation rate for a water level of 4 feet below the land surface. The water levels under the lowland area along the Republican River are in most localities from 3 to 12 feet below the land surface, and therefore the above coefficient was reduced to 1.0. U.S. Weather Bureau Climatological Data show that the average pan evaporation for the growing season in north-central Kansas was 56 inches for the period 1959-63.
If the above figures are reasonable for north-central Kansas, there would be about 12,000 acre-feet of water used annually by trees along the river between Hardy and Concordia. There are as many trees along the upland drainages as there are along the river lowlands, so. that the total estimated evapotranspiration by trees in the area is about 25,000 acre-feet or 0.4 inch annually between Hardy and Concordia. Because the trees obtain part of their water supply from soil moisture that never reaches the water table, only part of the 0.4 inch can be considered recharge.
Another estimate of the losses to evapotranspiration can be made from the base-flow data, considering that the effects of evapotranspiration are delayed in reaching the stream gage by 3 or 4 months and the difference in mean base flow between the growing and non-growing seasons might be the maximum losses to evapotranspiration in the basin. The base flow (mean of record) at Lovewell for the months of August through January averaged 5.81 cfs and for the months of February through July averaged 11.07 cfs. This difference, 5.26 cfs (or 0.2 inch), is the maximum loss. The difference at Endicott, Nebraska was 0.25 inch. Therefore, possibly 0.2 inch should be added to the 0.4 inch (Q80) recharge between Hardy and Concordia. The recharge rate in the Republican River area, then, is probably 0.6 inch, as indicated by both methods.
It should be noted that the above computations are for near natural conditions and for the total drainage area. The recharge potential along the valley bottoms is greater than the upland areas because of more sandy soils in the valley bottoms, Therefore, the recharge is probably greater than 0.6 inch in the lowland areas and less than that figure in the upland areas.
In 1963 there were 86 irrigation wells in Republic County and 101 in Cloud County. There were 12,300 acre-feet of ground water pumped in the Republican River drainage area for irrigation and municipal use in 1963 (Fig. 11). Eight thousand acre-feet were withdrawn above the gage at Concordia. A small amount was pumped from the Kansan deposits in north-central Republic County, but most of the pumpage was from the alluvial deposits in the lowlands along the river.
Figure 11--Withdrawals of ground water in the Republican River drainage basin.
In Kansas there is considerable ground water available along most of the major stream valleys. Several periods of deficient rainfall have prompted farmers in these areas to. develop irrigation systems utilizing ground water. Some of the water pumped from the valley aquifers would have been naturally discharged to the streams, and where the pumping level has been lowered to a point below the level of the stream, water moves directly from the stream into the aquifer. Pumping from wells has resulted in the interception of water moving toward the stream and has caused the surface water to move into the aquifer, thus affecting the flow of the stream. The following is an estimate of this effect on the flow of the Republican River.
Theis (1941) presented a method of estimating the effect of pumping a well on the flow of a nearby stream. The formula originally given contains a complex series. Conover (1954) devised a chart (Fig. 12) that allows a simple graphical solution of the formula. The estimates given later are based on data obtained from field tests in the area as applied to the chart.
Figure 12--Determination of percentage of pumped water being diverted from a river or drain. Explanation of terms below. (After Conover, 1954.)
The following assumptions are necessary in the use of the above method: (1) that the aquifer is homogeneous and isotropic; (2) that the aquifer and the stream are in free communication with each other (the river bed contains a minimum of silt so that ground-water flow from the stream is not retarded); (3) that constant pumping rates are maintained throughout the periods of time chosen; (4) that the lowering of the water level does not change the transmissibility; and (5) that there is sufficient flow in the river to satisfy the demands of pumping during the periods of time chosen.
The information needed to use the chart (Fig. 12) is as follows: (1) the coefficient of transmissibility (T), in gallons per day per foot, from Table 2; (2) the coefficient of storage (S), assumed to be 0.2; (3) the distance (a) between the well and the stream, scaled from well-location map; (4) the time of pumping (t) in years, assumed; and (5) the pumping rate (Q), in gallons per minute for each well reduced from the measured or reported rate by an assumed 20 percent to allow for return seepage from irrigation.
To use the diagram (Fig. 12), enter it either at the left or right with the distance from the stream (a). Proceed upward to the right or downward to the left parallel to the diagonal lines to the intersection with the S/T ratio (top of diagram), then proceed horizontally across the diagram to the intersection with the time (bottom of diagram). Read the percent from the diagonal lines, interpolating between lines if necessary. For example: If a = 0.15 mile, S/T= 2 X 10-6, and t=1 year, percent=91.
Using field data and the chart (Fig. 12), the percent of each well pumping rate supplied by the river was estimated at the end of 10, 20, 62, 124, 224, and 365 days. These percentages were entered in a table (not shown) and multiplied by the pumping rate of each well. The total quantities, in gallons per minute, obtained from the stream at the assumed times were computed and plotted on Figure 13.
Figure 13--Quantity of water supplied by streams to wells in the valley alluvium.
In summary, if all the irrigation wells in the river valley between Hardy and Concordia were pumped continuously at a constant rate of 66,000 gpm, the quantities supplied by the river would be:
Between Concordia and the Clay county line, if the total pumping rate were 38,000 gpm, the quantities supplied by the river would be:
In 1963, a year of below-normal rainfall, the average time irrigators pumped was 22 days. Figure 13 shows about 13,000 gpm or 29 cfs was being removed from the stream between Hardy and Concordia at the end of 22 days.
The area under the curves in Figure 13 is the volume pumped from the river. This would be 710 acre-feet between Hardy and Concordia and 420 acre-feet between Concordia and the Clay county line, or a total of 1,130 acre-feet if all the wells were pumped for 22 days. If these figures are correct, about 7,000 acre-feet of the 8,000 acre-feet (page 13) pumped above the gage at Concordia was removed from groundwater storage during the irrigation season. Figures 8, 9, and 10, show a decline of water level in the lowlands since 1960. However, as the aquifer was assumed to be full and water rejected for the estimate of recharge (page 13), it is estimated that the 7,000 acre-feet will be replaced by precipitation and seepage from the river during periods of higher precipitation.
Because of the history of high chloride content in water from irrigation wells in Cloud County, a sampling' program has been established to determine any changes in amount of chloride (Table 3). The chloride content increases in one or two wells during the pumping season, but there is very little change in chloride content from year to year. However, seven or more wells have been abandoned for irrigation use, owing to high chloride content. Because the abandoned wells were not pumped, comparable water samples were not available, and the changes in chloride content are not known.
Table 3--Chlorides in water from wells and-springs in the Republican River area, Kansas.
Well number |
Depth, ft |
Water- bearing unit* |
Date of sampling |
Chloride, ppm |
---|---|---|---|---|
Republic County | ||||
1-3W-3bc | 212 | Qd | 8-30-1962 | 12 |
1-3W-4dd | 111 | Qd | 7-30-1942 | 26 |
1-3W-10dd | 80 | Qd | 7-30-1942 | 18 |
1-3W-18cc | 171 | Qd | 7-30-1942 | 14 |
1-4W-4ba | 160 | Qd | 7-31-1942 | 34 |
1-4W-17dc | 55 | Qd | 7-30-1942 | 3 |
1-4W-31bc | 63 | Qd | 3-10-1942 | 24 |
1-4W-34ad | 115 | Qd | 7-30-1942 | 23 |
1-5W-6bb | ? | Qa | 7-30-1942 | 18 |
1-5W-14dc2 | 61 | Qa | 7-30-1942 | 20 |
1-5W-18ab | 49 | Qd | 7-1-1963 | 30 |
1-5W-18bb | 75 | Qd | 7-30-1942 | 25 |
1-5W-20ab | 160 | Qd | 6-27-1963 | 36 |
2-4W-7dd | 42 | Qa | 7-31-1942 | 26 |
2-5W-2bd1 | 19 | Qa | 7-30-1942 | 39 |
3-4W-9dd | 69 | Kg | 7-31-1942 | 57 |
3-4W-17db | 43 | Qa | 4-17-1942 | 46 |
3-4W-29da | 13 | Qa | 7-31-1942 | 118 |
3-4W-32da | 47 | Qa | 7-10-1963 | 138 |
3-5W-13dd | 56 | Kg | 7-31-1942 | 78 |
3-5W-16dd | 67 | Kc | 8-7-1944 | 168 |
3-5W-25bb | 64 | Kc | 7-31-1942 | 640 |
3-5W-32bb | 116 | Kd | 7-31-1942 | 1,320 |
4-4W-4db | 59 | Qa | 8-28-1963 | 48 |
4-4W-8ad | 60 | Qa | 7-9-1963 | 90 |
4-4W-8db | 40 | Qa | 7-9-1963 | 30 |
4-4W-8dd | 51 | Qa | 7-9-1963 | 42 |
4-4W-9ab | 72 | Qa | 7-10-1963 | 54 |
4-4W-9ca | 49 | Qa | 7-9-1963 | 90 |
4-4W-10cb | 44 | Qi | 7-2-1963 | 48 |
4-4W-16dab | 52 | Qw | 7-9-1963 | 36 |
4-4W-17da | 54 | Qa | 7-2-1963 | 66 |
4-4W-17dd | 60 | Qa | 7-9-1963 | 72 |
4-4W-21caa | 66 | Qw | 7-10-1963 | 42 |
4-4W-21cab | 66 | Qw | 7-9-1963 | 54 |
4-4W-22ca | 50 | Qi | 7-2-1963 | 30 |
4-4W-22cc | 56 | Qi | 7-9-1963 | 24 |
4-4W-27ddc | 59 | Qw | 6-19-1963 | 43 |
5-25-1964 | 50 | |||
7-20-1964 | 24 | |||
4-4W-29db | 53 | Qa | 7-10-1963 | 30 |
7-8-1964 | 36 | |||
4-4W-32cc2 | 35 | Qa | 7-31-1942 | 18 |
4-4W-33aa | 53 | Qa | 7-10-1963 | 42 |
7-8-1964 | 48 | |||
4-4W-33da | 63 | Qa | 7-20-1964 | 42 |
4-4W-33dc | 65 | Qa | 7-20-1964 | 84 |
4-4W-34baa | 52 | Qw | 8-25-1960 | 75 |
7-10-1963 | 30 | |||
7-8-1964 | 36 | |||
4-4W-34dbb | 49 | Qw | 8-25-1960 | 31 |
8-25-1961 | 40 | |||
5-25-1963 | 33 | |||
7-20-1964 | 36 | |||
4-5W-7cb | 42 | Kg | 7-31-1942 | 96 |
4-5W-23bc | 128 | Kd | 7-31-1942 | 1,655 |
4-5W-30ba | 84 | Kd | 7-31-1942 | 65 |
Cloud County | ||||
5-1W-15cc | 200 | Kd | 7-21-1964 | 54 |
5-1W-26ad2 | 158 | Kd | 8-4-1954 | 19 |
5-1W-30bc | Qa | 6-18-1963 | 24 | |
5-1W-30dcb1 | 71 | Qa | 8-15-1961 | 645 |
5-1W-30dcb2 | Qa | 5-25-1964 | 126 | |
7-21-1964 | 423 | |||
5-1W-31ac | 80 | Qw | 7-21-1964 | 135 |
5-1W-32bc | 74 | Qw | 8-16-1963 | 132 |
5-25-1964 | 51 | |||
7-21-1964 | 113 | |||
5-1W-32dc | 90 | Qw | 8-16-1963 | 54 |
7-21-1964 | 63 | |||
5-1W-34ddd | 60 | Qw | 1943 | 212 |
100 | Kd | 1943 | 450 | |
5-2W-15cb | 40 | Kd | 6-18-1963 | 46 |
5-2W-19bc | 93 | Qw | 6-20-1963 | 243 |
5-25-1964 | 94 | |||
7-21-1964 | 243 | |||
5-2W-19cbb | 71 | Qa | 1943 | 2,450 |
5-2W-20cca | 45 | Qa | 7-21-1964 | 45 |
5-2W-21ad | 50 | Qa | 8-27-1963 | 182 |
5-2W-21dd | 64 | Qa, Qk | 8-27-1963 | 510 |
5-25-1964 | 610 | |||
7-21-1964 | 370 | |||
5-2W-22ca | 55 | Qa | 7-21-1964 | 144 |
5-2W-25cb | 65 | Qw | 8-15-1961 | 65 |
5-2W-25cc | 72 | Qw | 1- -55 | 212 |
5-2W-26add | 80 | Qw | 1943 | 210 |
5-2W-26add | 99 | Qw | 1943 | 3,450 |
5-2W-28daa | 42 | Qa | 1943 | 23 |
65 | Qa | 1943 | 1,300 | |
72 | Qa | 1943 | 1,340 | |
80 | Qk | 1943 | 2,650 | |
5-2W-28da1 | 57 | Qa | 5-25-1964 | 572 |
7-21-1964 | 576 | |||
5-2W-28da2 | 48 | Qa | 5-25-1964 | 352 |
7-21-1964 | 387 | |||
5-2W-29ddb | 57 | Qa | 5-25-1964 | 572 |
7-21-1961 | 576 | |||
5-2W-29db | 48 | Qa | 5-25-1964 | 352 |
7-21-1964 | 387 | |||
5-2W-30bcd | 40 | Qa | 6-12-1954 | 368 |
8-15-1961 | 765 | |||
5-25-1964 | 136 | |||
7-21-1964 | 792 | |||
5-2W-31cc | 43 | Qd | 8-15-1963 | 18 |
5-2W-32cb | 50 | Qw | 8-16-1963 | 30 |
5-25-1964 | 36 | |||
7-21-1964 | 45 | |||
5-2W-32db | 54 | Qw | 8-16-1963 | 24 |
5-25-1964 | 34 | |||
7-21-1964 | 41 | |||
5-2W-34aab | 81 | Qw | 8-29-1963 | 90 |
5-25-1964 | 50 | |||
7-21-1964 | 99 | |||
5-2W-36bc | 40 | Qw | 6-18-1963 | 26 |
5-3W-15ab | 341 | Kd | 10-18-1955 | 16,000 |
5-3W-17abc | 100 | Qi | 8-25-1960 | 468 |
8-15-1961 | 390 | |||
7-6-1964 | 138 | |||
7-20-1964 | 372 | |||
5-3W-18bbb | 100 | Qi | 6-18-1954 | 44 |
5-3W-19bb1 | 90 | Kd | 1943 | 19 |
121 | Kd | 1943 | 850 | |
127 | Kd | 1943 | 1,900 | |
5-3W-19cb | 67 | Qa | 9- 8-1954 | 17 |
5-3W-19ddd | 52 | Qa | 1943 | 21 |
67 | Kd | 1943 | 26 | |
5-3W-20bbc | 70 | Qa | 1943 | 58 |
80 | Qk | 1943 | 413 | |
107 | Qk | 1943 | 3,760 | |
5-3W-21ca | 50 | Qa | 8-29-1963 | 24 |
5-3W-21cbc | 50 | Qw | 1943 | 59 |
71 | Qw | 1943 | 880 | |
5-3W-21dd | 47 | Qw | 1943 | 48 |
63 | Qw | 1943 | 89 | |
84 | Qk | 1943 | 2,880 | |
5-3W-22bad | 35 | Qi | 1943 | 230 |
71 | Qi | 1943 | 2,335 | |
5-3W-22bcc | 45 | Qw | 1943 | 167 |
50 | Qw | 1943 | 388 | |
60 | Qw | 1943 | 1,160 | |
87 | Qk | 1943 | 13,750 | |
5-3W-22dcb | 35 | Qa | 1943 | 331 |
65 | Qa | 1943 | 6,350 | |
5-3W-24dc | 55 | Qa | 7-21-1964 | 63 |
5-3W-25db | 48 | Qa | 5-25-1964 | 108 |
7-21-1964 | 63 | |||
5-3W-28bac | 36 | Qa | 1943 | 21 |
70 | Qk | 1943 | 86 | |
103 | Qk | 1943 | 4,360 | |
5-3W-28bb | 51 | Qa | 5-24-43 | 23 |
5-3W-28bbb | 50 | Qa | 1943 | 22 |
5-3W-28bbc | 50 | Qa | 1943 | 27 |
5-3W-28bbd | 42 | Qa | 1943 | 20 |
52 | Qa | 1943 | 30 | |
74 | Qa | 1943 | 228 | |
107 | Qk | 1943 | 5,040 | |
5-3W-28bbd2 | 20 | Qa | 1943 | 14 |
40 | Qa | 1943 | 22 | |
51 | Qa | 1943 | 27 | |
76 | Qk | 1943 | 1,400 | |
5-3W-29aac | 94 | Qk | 1943 | 3,500 |
5-3W-29bbc | 61 | Qa | 1943 | 45 |
5-3W-31bb | 37 | Qa | 6-3-1954 | 80 |
5-3W-32aa1 | 50 | Qa | 1- 2-45 | 72 |
5-3W-32aa2 | 50 | Qa | 1945 | 80 |
5-3W-32aa3 | 50 | Qa | 8-4-1954 | 110 |
5-3W-35abc | 65 | Qa | 8-15-1961 | 85 |
8-25-1963 | 72 | |||
5-25-1964 | 30 | |||
7-21-1964 | 90 | |||
5-3W-36ab | 85 | Qa | 8-15-1961 | 65 |
8-16-1963 | 85 | |||
5-25-1964 | 50 | |||
7-21-1964 | 54 | |||
5-3W-36bb | 74 | Qa | 8-15-1961 | 110 |
8-25-1963 | 84 | |||
5-25-1964 | 34 | |||
7-21-1964 | 81 | |||
5-4W-2bb | Qw | 7-20-1964 | 18 | |
5-4W-2ca1 | 48 | Qw | 6- 9-1964 | 30 |
5-4W-3abd | 59 | Qw | 8-25-1960 | 44 |
8-15-1961 | 40 | |||
5-4W-3dd | 68 | Qw | 8-23-1963 | 24 |
5-4W-4aac | 64 | Qw | 7-20-1964 | 72 |
5-4W-5cb | 33 | Qw | 6-25-1963 | 42 |
5-4W-7bd1 | 110 | Kd | 6-27-1963 | 660 |
5-4W-7dd | 39 | Qw | 6-25-1963 | 120 |
5-4W-8ad | 20 | Qw | 6-20-1963 | 238 |
5-4W-8bc | 40 | Qw | 6-25-1963 | 198 |
5-4W-8cc | 25 | Qw | 6-25-1963 | 144 |
5-4W-8dad | 60 | Qw | 8-15-1961 | 200 |
8-14-1963 | 210 | |||
7-21-1964 | 198 | |||
5-4W-8dda | 60 | Qw | 8-15-1961 | 80 |
7-21-1964 | 150 | |||
5-4W-9cca | 75 | Qw | 5-13-1960 | 35 |
8-25-1960 | 13 | |||
8-24-1963 | 30 | |||
5-25-1964 | 32 | |||
5-4W-10ba | 54 | Qw | 8-25-1960 | 31 |
5-4W-11ad1 | 39 | Qw | 7-20-1964 | 18 |
5-4W-11ad2 | 38 | Qw | 7-20-1964 | 36 |
5-4W-13bbb | 39 | Qw | 1943 | 25 |
44 | Qw | 1943 | 43 | |
5-4W-13bd | 40 | Qw | 8-15-1961 | 35 |
5-25-1964 | 18 | |||
7-8-1964 | 24 | |||
7-20-1964 | 38 | |||
5-4W-13dad | 53 | Qw | 8-15-1961 | 85 |
8-23-1963 | 90 | |||
7-7-1964 | 60 | |||
7-20-1964 | 90 | |||
5-4W-14aa | 33 | Qw | 7-20-1964 | 30 |
5-4W-14abb | 56 | Qw | 1943 | 47 |
5-4W-14da | 48 | Qw | 5-25-1964 | 27 |
7-20-1964 | 36 | |||
5-4W-15aba | 69 | Qa | 5-13-1960 | 95 |
8-25-1960 | 75 | |||
8-15-1961 | 78 | |||
5-25-1964 | 112 | |||
7-21-1964 | 72 | |||
5-4W-15cad | 72 | Qa | 5-13-1960 | 287 |
8-25-1960 | 200 | |||
8-15-1961 | 300 | |||
7-10-1963 | 390 | |||
8-11-1963 | 414 | |||
5-4W-15cad | 5-25-1964 | 336 | ||
7-21-1964 | 420 | |||
5-4W-15da | 70 | Qa | 8-25-1960 | 144 |
8-15-1961 | 170 | |||
7-18-1963 | 152 | |||
7-21-1964 | 270 | |||
5-4W-15ddd | 65 | Qw | 1943 | 450 |
117 | Qk | 1943 | 1,240 | |
5-4W-16bd | 83 | Qw | 5-13-1960 | 100 |
8-25-1960 | 94 | |||
8-15-1961 | 100 | |||
7-21-1964 | 90 | |||
5-4W-16ca | 85 | Qw, Qi | 5-13-1960 | 435 |
8-25-1960 | 440 | |||
8-15-1961 | 485 | |||
7- -1963 | 378 | |||
7- -1963 | 498 | |||
7- -1963 | 696 | |||
5-25-1964 | 680 | |||
5-4W-16cb | 45 | Qw | 5-13-1960 | 75 |
8-25-1960 | 75 | |||
8-15-1961 | 125 | |||
8-24-1963 | 84 | |||
5-25-1964 | 76 | |||
7-21-1964 | 96 | |||
5-4W-16dc | 25 | Qw | 8-20-1963 | 42 |
7-21-1964 | 60 | |||
5-4W-16dd | 60 | Qw | 5-13-1960 | 37 |
8-25-1960 | 75 | |||
8-15-1961 | 145 | |||
8-22-1963 | 78 | |||
5-4W-17aa | 64 | Qw | 5-13-1960 | 81 |
8-25-1960 | 100 | |||
8-15-1961 | 130 | |||
8-24-1963 | 132 | |||
5-25-1964 | 100 | |||
7-21-1964 | 138 | |||
5-4W-18bb1 | 54 | Qi | 6-25-1963 | 132 |
5-4W-18bb2 | 60 | Kd | 6-25-1963 | 282 |
5-4W-18bc | 47 | Qi | 6-25-1963 | 138 |
5-4W-18cb | 60 | Qi | 6-25-1963 | 78 |
5-4W-18dd | 48 | Kd | 6-25-1963 | 498 |
5-4W-19ad | 50 | Qi | 6-25-1963 | 474 |
5-4W-19da | 36 | Qi | 6-25-1963 | 564 |
5-4W-20bb | 49 | Qi | 6-25-1963 | 552 |
5-4W-21ba | 59 | Qw | 5-13-1960 | 112 |
8-25-1960 | 206 | |||
8-15-1961 | 260 | |||
8-22-1963 | 282 | |||
5-25-1964 | 70 | |||
5-4W-21bd2 | 24 | Qw | 6-25-1963 | 354 |
7-21-1964 | 432 | |||
5-4W-21db | Qw | 6-25-1963 | 450 | |
5-4W-22ab | 68 | Qw | 5-13-1960 | 100 |
8-25-1960 | 167 | |||
8-15-1961 | 155 | |||
8-14-1963 | 150 | |||
7-21-1964 | 150 | |||
5-5W-4aab | 80 | Kd | 11- 5-53 | 205 |
160 | Kd | 11-17-1953 | 16,400 | |
402 | Kd | 11-17-1953 | 17,800 | |
5-5W-4bb | 53 | Qk | 10-30-1953 | 9,310 |
5-5W-7cc | 55 | Qk | 5-18-1954 | 1,150 |
5-5W-11ad | 168 | Kd | 6-27-1963 | 60 |
5-5W-12ad | 130 | Kd | 6-28-1963 | 300 |
5-5W-12bc1 | 40 | Qi | 6-28-1963 | 96 |
5-5W-22da | 140 | Qi | 7-7-1953 | 43 |
5-5W-24dd | 57 | Qk | 5-20-1954 | 28 |
6-1W-2ca | 84 | Qw, Kd | 8-26-1963 | 18 |
6-1W-3aa | 41 | Qa | 6-15-1954 | 21 |
77 | Qk | 6-15-1954 | 19 | |
6-1W-4bc2 | 86 | Qw | 8-27-1963 | 42 |
6-1W-10cc | 87 | Kd | 3-4-1954 | 13 |
6-1W-12ab | 63 | Qw | 8-26-1963 | 24 |
*Qd, Pleistocene deposits, undifferentiated; Qa, Recent alluvium; Qw, Wisconsinan terrace deposits; Qi, Illinoisan terrace deposits; Qk, Kansan deposits; Kd, Dakota Formation; Kg, Greenhorn Limestone; Kc, Carlile Shale. |
The Dakota Formation in most of northwestern Cloud County contains water high in chloride, 250 ppm (parts per million) or higher (Pl. 4). The water in the Dakota Formation moves into the Kansan and alluvial deposits (Fig. 14) in the subsurface, and therefore most of the Kansan deposits and the basal part of the alluvial deposits along the Republican River in Cloud County contain brackish water. In some areas (Pl. 4) along the Republican River, water from some wells contains more chloride than is tolerable for irrigation and other uses.
Figure 14--Diagrammatic cross sections D-D' and E-E', northwestern Cloud County, Kansas.
Diagrammatic sections for an area west of Concordia are presented in Figure 14. The brackish water is flowing into the area from the west almost parallel to cross section E-E'. As the wells in sec. 16, 17, and 20, T 5 S, R 4 W, are pumped, the brackish water moves northward and upward into the wells, and the chloride content of water from the southern-most wells in section D-D' will increase. However, the Republican River, which normally contains water of low chloride content, recharges the aquifer when the water level in wells is lowered below the river level. This provides water of low chloride content to the wells near the river; whereas, the water from the river is intercepted by pumping wells before reaching the southernmost wells. Thus, the southernmost wells pick up the brackish water from the lower parts of the aquifers.
In the area northeast of Concordia, brackish water from the Dakota Formation moves from the north into the alluvial deposits in the subsurface. This underflow accounts for the high chloride content in the alluvial deposits in T 5 S, R 3 W. East of Salt Creek the underflow is less brackish. As the brackish water moves eastward along the bottom of the valley alluvium, recharge from rainfall and the less brackish underflow from the north and south dilutes the brackish water, and only a small amount of brackish water occurs as a narrow strip in T 4 S, Rs 1 and 2 W. In general, most of the Kansan deposits in the Republican River valley in Cloud County contain brackish water. Thus, very few irrigation wells are drilled into these deposits. Thin clay layers in the lower parts of the alluvial deposits above the Kansan deposits may retard the upward movement of brackish water, provided the wells do not penetrate the clay layers.
The Republican River area is divided into two general categories in relationship to the ground-water aquifers. In the lowland areas, large quantities of water are available from the alluvial deposits. In the upland areas, water can be obtained from silts, clays, and silty gravels of Pleistocene age overlying the Cretaceous rocks or from the Cretaceous rocks. However, the application of surface-water irrigation has raised the water level in some of the upland areas causing flooding of pump pits at well sites and waterlogging of fields. Only the upper part of the Cretaceous material yields water suitable for most uses, as the water becomes more saline with depth.
Data from aquifer tests indicate that the coefficient of transmissibility ranges from 10,000 to 320,000 gpd/ft and the coefficient of permeability ranges from 800 to 6,300 gpd/ft2. Coefficient of storage was not determined from the short aquifer tests but was assumed from experience in other areas.
Water levels dropped in the upland areas during the period 1953-56, rose with increased precipitation during the period 1956-58, and rose considerably in the areas irrigated by surface water after 1958. Waterlogging has occurred in some of those areas. Water levels in the lowland areas fluctuate with the rate of discharge of the Republican River and with the local pumping rate.
The alluvial deposits above the Kansan deposits contain about 580,000 acre-feet of water in storage. If water levels are drawn down due to pumping, the aquifers become thin and no longer yield sufficient water for irrigation. Therefore, part of the water in storage is unavailable for irrigation.
Recharge from precipitation was computed from streamflow records to be about 0.6 inch per year over the area. An estimated 0.2 inch is lost to evapotranspiration before reaching the streams. Recharge in the lowland areas is probably greater than in the upland areas.
Withdrawal of ground water in the lowlands was 7,600 acre-feet in 1958 and 12,300 acre-feet in 1963. The theoretical quantity of water removed from the Republican River by the pumping of ground water between Hardy and Concordia was computed to be 710 acre-feet in 1963.
Chlorides in irrigation water are a problem in northern Cloud County. However, suitable water can be obtained from aquifers, which are stratigraphically higher than Kansan deposits, in most of the lowland areas.
The following recommendations are included so that sufficient data will be available for future analyses of the hydrology of the area, either by the digital computers, electronic analog models, or other methods. These types of analyses were beyond the scope of this report or the need for additional data was recognized too late to be included in the study.
The measurement of water levels in the area should be continued at the present intervals with the same areal coverage. However, four or five additional observation wells should be drilled along the upland on the east side of the Republican River for the purpose of comparing fluctuations of water levels in similar geologic formations outside the area of influence of the irrigation by surface water. The approximate locations of these wells, depending on the geology found when drilled, should be:
The measurement program of the low flows of the Republican River between Hardy and Concordia should be extended so that more accurate estimates of gains or losses in this reach are available. This may include an investigation by statistical methods as to the type or types of field data needed.
The collection of data on the chlorides in water should be continued on the present annual monitoring basis.
Logs of 22 test holes drilled in the Republican River area were selected to represent the different types of materials encountered. Eleven of these test holes were drilled by the State and Federal Geological Surveys and are headed "Sample log of test hole augered...." These test holes were logged by the author during drilling. Nine of the test holes were drilled and logged by the U.S. Bureau of Reclamation; these are headed "Log of test hole drilled by U.S. Bureau of Reclamation...." The remaining test holes were drilled and logged by commercial well drillers and are headed "Driller's log of test hole drilled by...."
1-3W-5bc--Driller's log of test hole in SW NW sec. 5, T 1 S, R 3 W near center of NW sec.; drilled by Don Barney for Edwin Tientjen, June 1958. Altitude of land surface, 1,662 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series, undifferentiated | ||||||
Loam | 2 | 2 | ||||
Clay, yellowish-brown | 7 | 9 | ||||
Clay, brown | 8 | 17 | ||||
Sand, brown, clay | 6 | 23 | ||||
Clay, brown | 39 | 62 | ||||
Sand, fine | 23 | 85 | ||||
Clay | 1 | 86 | ||||
Sand, fine | 7 | 93 | ||||
Clay, gray | 14 | 107 | ||||
Clay, brown, soft | 6 | 113 | ||||
Clay, brown | 9 | 122 | ||||
Sand, fine, and gravel | 96 | 218 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, black | 2 | 220 |
1-4W-31cc (U.S.B.R. 164)--Log of test hole in SW SW sec. 31, T 1 S, R 4 W, 50 feet north and 350 feet east of SW cor. sec.; drilled by U.S. Bureau of Reclamation, October 1957. Altitude of land surface, 1,496 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Illinoisan Stage | ||||||
Crete and Loveland formations | ||||||
Silt | 5 | 5 | ||||
Sand, fine, slight amount silt | 3 | 8 | ||||
Silt | 12 | 20 | ||||
Silt and fine sand | 2 | 22 | ||||
Sand, fine, clean; loose | 4 | 26 | ||||
Sand, fine to coarse; loose | 10 | 36 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, blue; firm | 2+ | 38+ |
1-4W-31dc--Sample log of test hole in SW SE sec. 31, T 1 S, R 4 W, 20 feet north and 100 feet east of S2 cor. sec.; augered, November 29, 1962. Altitude of land surface, 1,514 (estimated) feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Illinoisan Stage | ||||||
Crete and Loveland formations, undifferentiated | ||||||
Topsoil, black | 4 | 4 | ||||
Clay, bluish-black | 2 | 6 | ||||
Clay, tan | 5 | 11 | ||||
Clay, silty, tan | 9 | 20 | ||||
Kansan Stage | ||||||
Grand Island and Sappa formations, undifferentiated | ||||||
Clay, silty, dark-brown | 4 | 24 | ||||
Sand, fine to medium, tannish-brown | 2 | 26 | ||||
Clay, brownish-red | 3 | 29 | ||||
Gravel and clay strips | 6 | 35 | ||||
Sand, coarse, tan | 5 | 40 | ||||
Sand, coarse, and pea-sized gravel | 4 | 44 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, bluish-black, hard | 1 | 45 |
1-5W-9ddd--Sample log of test hole in SE SE SE sec. 9, T 1 S, R 5 W, 20 feet north and 30 feet west of SE cor. sec.; augered, June 1963. Altitude of land surface, 1,501 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Recent Stage (alluvium) | ||||||
Sand, fine, silty, tannish-brown | 5 | 5 | ||||
Sand, coarse, tan | 5 | 10 | ||||
Sand and gravel, bluish-gray | 8 | 18 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, black; drilled hard | 1+ | 19+ |
1-5W-10aaa--Sample log of test hole in NE NE NE sec. 10, T 1 S, R 5 W, 40 feet south and 35 feet west of NE cor. sec.; augered, June 1965. Altitude of land surface, 1,550 (estimated) feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan and Illinoisan stages | ||||||
Peoria and Loveland formations, undifferentiated | ||||||
Topsoil, brown | 1 | 1 | ||||
Clay, silty, black | 5 | 6 | ||||
Clay, silty, brown | 2 | 8 | ||||
Pleistocene fluvial deposits, undifferentiated | ||||||
Sand, coarse, brownish-tan; hard to drill | 13 | 21 | ||||
Sand and pea-sized gravel, tannish-brown | 4 | 25 | ||||
Clay, gravel, and sand layers, blue | 2 | 27 | ||||
Sand, coarse, and gravel, blue; with some clay | 15 | 42 | ||||
Gravel, and blue clay; drilled hard | 21 | 63 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, black | 2+ | 65+ |
1-5W-16ccc--Log of test hole in SW SW SW sec. 16, T 1 S, R 5 W, near SW cor. sec.; drilled by U.S. Bureau of Reclamation, May 1961. Altitude of land surface, 1,510 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series, undifferentiated | ||||||
Silt, dark-brown; drilled easy | 5 | 5 | ||||
Silt, light-brown; drilled easy | 4 | 9 | ||||
Clay, silty, dark-gray; drilled easy | 3 | 12 | ||||
Clay, silty, light-gray; drilled easy | 3 | 15 | ||||
Sand, very fine, gray; loose | 8 | 23 | ||||
Sand, fine to medium, gray; loose | 10 | 33 | ||||
Sand, fine to coarse, bluish-gray; loose | 5 | 38 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, blue; firm | 2+ | 40+ |
1-5W-36dc (U.S.B.R. 163 F)--Log of test hole in SW SE sec. 36, T 1 S, R 5 W, 100 feet north and 1,180 feet west of SE cor. sec.; drilled by U.S. Bureau of Reclamation, January 1958. Altitude of land surface, 1,486 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Illinoisan Stage | ||||||
Crete and Loveland formations | ||||||
Silt | 4 | 4 | ||||
Sand, fine, silty; loose | 2 | 6 | ||||
Silt | 1 | 7 | ||||
Sand, fine, silty; loose | 1 | 8 | ||||
Silt; small amount fine sand | 9 | 17 | ||||
Silt | 1 | 18 | ||||
Clay, silty, compact | 1 | 19 | ||||
Sand, fine; small amount silt | 1 | 20 | ||||
Silt | 2 | 22 | ||||
Sand, fine, silty | 3 | 25 | ||||
Sand, fine to coarse; loose | 3 | 28 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, blue; firm | 2 | 30 |
1-5W-35dd (U.S.B.R. 162 B)--Log of test hole in SE SE sec. 35, T 1 S, R 5 W, 100 feet north and 160 feet west of SW cor. sec.; drilled by U.S. Bureau of Reclamation, 1957. Altitude of land surface, 1,478 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Recent Stage (alluvium) | ||||||
Sand, very fine, silty; loose | 2 | 2 | ||||
Sand, very fine, some silt; loose | 2 | 4 | ||||
Sand, fine | 7 | 11 | ||||
Sand, fine to coarse; loose | 6 | 17 | ||||
Sand, fine to coarse; silty, small pieces weathered shale | 7 | 24 | ||||
Sand, fine to coarse, some small gravel, small pieces weathered shale | 2 | 26 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, blue; firm | 2 | 28 |
2-4W-5bbb--Sample log of test hole in NW NW NW sec. 5, T 2 S, R 4 W, 20 feet south and 15 feet east 01 NW cor. sec.; augered, June 1963. Altitude of lane surface, 1,545 (estimated) feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan and Illinoisan stages | ||||||
Peoria and Loveland formations, undifferentiated | ||||||
Silt, tan | 10 | 10 | ||||
Clay, silty, tannish-yellow | 6 | 16 | ||||
Sand, very fine, tannish-white; drilled hard | 9 | 25 | ||||
Sand, medium, tan | 9 | 34 | ||||
Sand, medium, silty; grayish-tan | 5 | 39 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, sandy, black; drilled hard | 2+ | 41+ |
2-5W-1ba (U.S.B.R. 163)--Log of test hole in NE m sec. 1, T 2 S, R 5 W, 10 feet south and 1,300 feet east of NW cor. sec.; drilled by U.S. Bureau of Reclamation 1957. Altitude of land surface, 1,476 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Recent Stage (alluvium) | ||||||
Sand, very fine, silty; loose | 5 | 5 | ||||
Sand, fine; loose | 3 | 8 | ||||
Sand, fine to medium; loose | 11 | 19 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, blue; firm | 2 | 21 |
2-5W-20aa--Log of test hole in NE NE sec. 20, T 2 S, R 5 W, near NE cor. sec.; drilled by U.S. Bureau of Reclamation, 1955. Altitude of land surface, 1,554 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan and Illinoisan stages | ||||||
Peoria and Loveland formations, undifferentiated | ||||||
Silt, clayey, dark-brown | 2 | 2 | ||||
Clay, silty, brown | 1 | 3 | ||||
Silt, light-gray, rusty streaks | 8 | 11 | ||||
Silt, dark-brown | 5 | 16 | ||||
Clay, silty, light grayish-brown | 9 | 25 | ||||
Clay, silty, brown | 4 | 29 | ||||
Pleistocene Series, undifferentiated | ||||||
Clay, light-yellow, and weathered shale | 11 | 40 |
3-4W-8cc3--Sample log of test hole in SW SW sec. 8, T 3 S, R 4 W, 100 feet northeast of well 8cc1; augered, November 1962. Altitude of land surface, 1,437 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Recent Stage (alluvium) | ||||||
Topsoil, black | 2 | 2 | ||||
Sand, coarse, brown | 20 | 22 | ||||
Sand, coarse, and gravel, bluish-gray | 27 | 49 | ||||
Clay, blue | 1+ | 50+ |
3-5W-16bb--Log of test hole in NW NW sec. 16, T 3 S, R 5 W, near NW cor. sec.; drilled by U.S. Bureau of Reclamation, 1956. Altitude of land surface, 1,511 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan and Illinoisan stages | ||||||
Peoria and Loveland formations, undifferentiated | ||||||
Clay, clark-brown | 2 | 2 | ||||
Clay, dark-gray | 2 | 4 | ||||
Silt, light rusty-brown | 7 | 11 | ||||
Pleistocene Series, undifferentiated | ||||||
Clay, dark-gray | 5 | 16 | ||||
Clay, light-brown | 12 | 28 | ||||
Clay, silty, light-brown | 7 | 35 | ||||
Clay, yellowish-brown | 13 | 48 | ||||
Chalk, weathered, yellow | 18 | 66 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Carlile Shale | ||||||
Shale, blue | 1+ | 67+ |
3-5W-20ad--Log of test hole in SE NE sec. 20, T 3 S, R 5 W, near E2; cor. sec.; drilled by U.S. Bureau of Reclamation, 1961. Altitude of land surface, 1,499 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan and Illinoisan stages | ||||||
Peoria and Loveland formations, undifferentiated | ||||||
Clay, silty, dark-brown | 4 | 4 | ||||
Silt, light grayish-brown, rusty streaks | 6 | 10 | ||||
Clay, silty, reddish-brown | 25 | 35 | ||||
Clay, yellow, and chalk fragments | 1 | 36 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Greenhorn Limestone | ||||||
Chalk, weathered, yellow | 1+ | 37+ |
4-4W-4dc2--Sample log of test hole in SW SE sec. 4, T 4 S, R 4 W, 0.1 mile north and 0.1 mile east of S2; cor. sec.; augered, November 1962. Altitude of land surface, 1,431 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan Stage (terrace deposits) | ||||||
Topsoil | 5 | 5 | ||||
Clay, silty, black | 9 | 14 | ||||
Clay, silty, tan | 2 | 16 | ||||
Silt, tan, and fine sand | 7 | 23 | ||||
Sand, fine, silty, grayish-tan | 7 | 30 | ||||
Sand, medium to coarse, silty, gray | 10 | 40 | ||||
Sand, coarse, gray | 5 | 45 | ||||
Sand, coarse, and fine gravel, gray | 5 | 50 | ||||
Gravel and coarse sand, gray | 17 | 67 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Graneros Shale | ||||||
Shale, yellowish-brown; drilled hard | 6+ | 73+ |
4-4W-21cab--Driller's log of test hole in NW NE SW sec. 21, T 4 S, R 4 W; drilled by Ben Lervold, at irrigation well for Lloyd Blosser, April 1954. Altitude of land surface, 1,412 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan Stage (terrace deposits) | ||||||
Loam | 8 | 8 | ||||
Clay and sand | 14 | 22 | ||||
Gravel, medium, and sand | 8 | 30 | ||||
Gravel, coarse | 38 | 68 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Graneros Shale | ||||||
Clay, blue | 22 | 90+ |
4-4W -30cc--Sample log of test hole in SW SW sec. 30, T 4 S, R 4 W, 160 feet north and 30 feet east of SW cor. sec.; augered, November 1962. Altitude of land surface, 1,424 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Recent Stage (alluvium) | ||||||
Topsoil (and road fill), black | 10 | 10 | ||||
Clay, brown | 2 | 12 | ||||
Clay, silty, brown | 8 | 20 | ||||
Clay, brown, and silty clay layers | 7 | 27 | ||||
Sand, fine, brown | 1 | 28 | ||||
Clay, brown, and silty clay layers | 11 | 39 | ||||
Clay, silty, brown | 27 | 66 | ||||
Clay, silty, brown; drilled hard | 4 | 70 | ||||
Clay, silty brown; layers of fine yellow sand | 8+ | 78+ |
4-5W-16cc--Log of test hole in SW SW sec. 16, T 4 S, R 5 W, near SW cor. sec.; drilled by U.S. Bureau of Reclamation, 1956. Altitude of land surface, 1,500 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan and Illinoisan stages | ||||||
Peoria and Loveland formations, undifferentiated | ||||||
Silt, brown | 5 | 5 | ||||
Clay, silty, brown | 3 | 8 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Greenhorn Limestone | ||||||
Chalk, weathered, yellow; some hard layers | 14+ | 22+ |
4-5W-19bbb--Sample log of test hole in NW NW NW sec. 19, T 4 S, R 5 W, 30 feet south and 35 feet east of NW cor. sec.; augered, June 1963. Altitude of land surface, 1,396 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series, undifferentiated | ||||||
Topsoil, black | 2 | 2 | ||||
Clay, tan, silty; drilled hard | 8 | 10 | ||||
Clay and fine silty sand layers | 9 | 19 | ||||
Clay, blue | 3 | 22 | ||||
Silt, bluish-gray, clayey | 12 | 34 | ||||
Clay and silt, bluish-gray | 7 | 41 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Graneros Shale | ||||||
Sandstone and shale, blue | 2+ | 43+ |
4-5W-32da--Sample log of test hole in NE SE sec. 32, T 4 S, R 5 W, 35 feet south and 35 feet west of E2 cor. sec.; augered, June 1963. Altitude of land surface, 1,395 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series, undifferentiated | ||||||
Topsoil, black | 2 | 2 | ||||
Clay, silty, gray | 3 | 5 | ||||
Silt, sandy, brown | 3 | 8 | ||||
Silt, gray | 4 | 12 | ||||
Sand, very fine, gray | 4 | 16 | ||||
Silt, gray | 4 | 20 | ||||
Silt, brown, and fine sand layers | 7 | 27 | ||||
Clay, brown | 5 | 32 | ||||
Silt and very fine sand | 6 | 38 | ||||
Sand, very fine, silty, brownish-tan | 14 | 52 | ||||
Silt, gray | 7 | 59 | ||||
Cretaceous System | ||||||
Upper Cretaceous Series | ||||||
Graneros Shale | ||||||
Shale, blue; drilled hard | 4+ | 63+ |
5-4W-26bc--Sample log of test hole in SW NW sec. 26, T 5 S, R 4 W, 60 feet east of W2 cor. sec.; augered, November 1962. Altitude of land surface, 1,375 feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan Stage (terrace deposits) | ||||||
Topsoil, black | 5 | 5 | ||||
Sand, fine, brown | 3 | 8 | ||||
Clay, gray | 2 | 10 | ||||
Sand, fine, brown | 8 | 18 | ||||
Clay, silt, and fine sand, gray | 5 | 23 | ||||
Silt and fine sand, gray | 7 | 30 | ||||
Sand, very fine, silty, brown | 5 | 35 | ||||
Sand, very fine, silty, bluish-gray | 13 | 48 | ||||
Sand, coarse, and fine gravel | 3 | 51 | ||||
Cretaceous System | ||||||
Lower (?) Cretaceous Series | ||||||
Dakota Formation | ||||||
Shale, weathered, blue | 4 | 55 | ||||
Shale, blue | 2+ | 57+ |
5-5W-2cd--Sample log of test hole in SE SW sec. 2, T 5 S, R 5 W, 30 feet north and 0.45 mile west of SE cor. sec.; augered, June 1962. Altitude of land surface, 1,432 (estimated) feet. | Thickness, feet |
Depth, feet |
||||
---|---|---|---|---|---|---|
Quaternary System | ||||||
Pleistocene Series | ||||||
Wisconsinan Stage (terrace deposits) | ||||||
Topsoil, black, and silty clay loam | 3 | 3 | ||||
Clay, silty, tan | 8 | 11 | ||||
Sand, very fine, silty, clayey; some sandstone chips, tannish-white | 7 | 18 | ||||
Clay, brown, hard | 1 | 19 | ||||
Silt and sand, very fine, tan | 8 | 27 | ||||
Clay and silt layers | 3 | 30 | ||||
Silt and very fine sand, tan | 3 | 33 | ||||
Silt and very fine sand, tan; some layers drilled hard | 4 | 37 | ||||
Cretaceous System | ||||||
Lower (?) Cretaceous Series | ||||||
Dakota Formation | ||||||
Clay, blue, and tan sandstone stringers | 5+ | 42+ |
Bayne, C. K., and Walters, K. L., 1959, Geology and ground-water resources of Cloud County, Kansas: Kansas Geol. Survey, Bull. 139, p. 1-144. [available online]
Blaney, H. F., 1957, Relation of pan evaporation to evapotranspiration by phreatophytes and hydrophytes: Phreatophyte Subcommittee of Pacific Southwest Inter-Agency Committee, Symposium on Phreatophytes, Sacramento, Calif., Feb. 14-15, p. 1-52.
Buck, L. P., Van Horn, Richard, and Young, R. G., 1951, Construction materials in Cloud County, Kansas: U.S. Geol. Survey, Circ. 88, p. 1-20. [available online]
Busby, M. W., and Armentrout, G. W., 1965, Kansas streamflow characteristics, pt. 6A, Base flow data: Kansas Water Resources Board Tech. Rept, no. 6A, p. 1-207.
Byrne, F. E., Houston, M. S., and Mudge, M. R., 1950, Construction materials in Jewell County, Kansas: U.S. Geol. Survey, Circ. 38, p. 1-21. [available online]
Conover, C. S., 1954, Ground-water conditions in the Rincon and Mesilla valleys and adjacent areas in New Mexico: U.S. Geol. Survey, Water-Supply Paper 1230, p. 1-200, fig. 1-15. [available online]
Cooper, H. H., Jr., and Jacob, C. E., 1946, A generalized graphical method for evaluating formation constants and summarizing well-field history: Am. Geophys. Union Trans., v. 27, p. 526-534, fig. 1-5.
Darton, N. H., 1905, Preliminary report on geology and underground water resources of the central Great Plains: U.S. Geol. Survey, Prof. Paper 32, p. 1-433. [available online]
Fishel, V. C., 1948, Ground-water resources of Republic County and northern Cloud County, Kansas: Kansas Geol. Survey, Bull. 73, p. 1-194. [available online]
Fishel, V. C., and Leonard, A. R., 1955, Geology and ground-water resources of Jewell County, Kansas: Kansas Geol. Survey, Bull. 115, p, 1-152. [available online]
Franks, P. C., 1966, Petrology and stratigraphy of the Kiowa and Dakota formations (basal Cretaceous), north-central Kansas: Unpublished Ph.D. dissertation, Dept. Geol., Univ. Kansas, v. 1, 218 p., v. 2, plates.
Furness, L. W., 1959, Kansas streamflow characteristics, part 1, flow duration: State of Kansas Water Resources Board Tech. Rept. no. 1, p. 1-213.
Hatten, D. E., 1962, Stratigraphy of the Carlile Shale (Upper Cretaceous) in Kansas: Kansas Geol. Survey, Bull. 156, p. 1-155. [available online]
Haworth, Erasmus, 1913, Special report on well waters in Kansas: Kansas Geol. Survey, Bull. 1, p. 1-103.
Jewett, J. M., 1959, Graphic column and classification of rocks in Kansas: Kansas Geological Survey, chart, 1 sheet.
Kansas Water Resources Board, 1961, Preliminary appraisal of Kansas water problems, sec. 9 Lower Republican Unit: Kansas Water Resources Board, State Water Plan Studies, pt. A, p. 1-99.
Logan, W. N., 1897, The upper Cretaceous of Kansas: Kansas Geol. Survey, v. 2, p. 199-234, fig. 10-11, pl. 28-34.
Moore, R. C., Lohman, S. W., Frye, J. C., Waite, H. A., McLaughlin, T. G., and Latta, Bruce, 1940, Groundwater resources of Kansas: Kansas Geol. Survey, Bull. 27, p. 1-112.
Plummer, Norman, and Romary, J. F., 1942, Stratigraphy of the pre-Greenhorn Cretaceous beds of Kansas: Kansas Geol. Survey, Bull. 41, pt. 9, p. 313-348. [available online]
Schoewe, W. H., 1952, Coal resources of the Cretaceous System (Dakota Formation) in central Kansas: Kansas Geol. Survey, Bull. 96, pt. 2, p. 69-156. [available online]
Theis, C. V., 1935, The relation between the lowering of the piezometric surface and the rate and duration of discharge of a well using ground-water storage: Am. Geophys, Union Trans., v. 16, pt. 2, p. 519-524.
Theis, C. V., 1941, The effect of a well on the flow of a nearby stream: Am. Geophys. Union Trans., v. 22, pt. 3, p. 734-738.
Wing, M. E., 1930, The Geology of Cloud and Republic Counties, Kansas: Kansas Geol. Survey, Bull. 15, p. 1-49. [available online]
Kansas Geological Survey
Placed on web March 26, 2013; originally published in April 1968.
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