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UNITED STATES DEPARTMENT OF THE INTERIOR

GEOLOGICAL SURVEY • 7.=

R.

TEST-OBSERVATION WELL NEAR DAVENPORT, WASHINGTON:

DESCRIPTION AND PRELIMINARY RESULTS

By A

.r

D. A. Myers

4

Prepared in cooperation with the State of Washington Department of Ecology

g

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174.

OPEN-FILE REPORT

I

Tacoma, Washington 1972

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UNITED STATES DEPARTMENT OF THE INTERIOR

GEOLOGICAL SURVEY

TEST-OBSERVATION WELL NEAR DAVENPORT, WASHINGTON:

DESCRIPTION AND PRELIMINARY RESULTS

By

D. A. Myers , 9c;

Prepared in cooperation with the State of Washington Department of Ecology

OPEN-FILE REPORT

218144 Tacoma, Washington

1972

a.otoq,AL suki„,, •

FEB 2 (6 19/3

CONTENTS

Page

Abstract- 1

Introduction 3

Background and ground-water problems of the area 8

Results of the study 9

Construction of the well 9

Pumping tests 14

Quality of water 17

Geophysical logs 17

Additional information expected 21

References cited 23

II

ILLUSTRATIONS

Page

FIGURE 1„ Map of Washington showing locations of

test-observation wells 5

2. Diagrammatic sketch of test-observation

wen 10

3. Geophysical logs 19

TABLES

TABLE 1. Depth to water during drilling 7

2. Driller's log of well 10

3. Water levels in piezometer pipes,

Sept. 8, 1971 15

4. Chemical quality of water from different

depths in well 18

III

TEST-OBSERVATION WELL NEAR DAVENPORT, WASHINGTON:

DESCRIPTION AND PRELIMINARY RESULTS

By D. A. Myers

ABSTRACT

The 750-foot test-observation well drilled near Davenport,

Wash., is one of several drilled to date (1972) to provide

information on ground-water conditions in selected areas of

the State. The well provides information on aquifer charac-

teristics in this area which are not available from existing

deep irrigation wells. The well was drilled by air-rotary

methods and penetrates eight aquifer zones (A through H);

the upper 75 feet of the well is cased, and the remainder of

the hole is open in basalt.

Test pumping during drilling showed that the well had

specific capacities of (1) 4-8 gpm (gallons per minute) per

foot of drawdown when at the 255-foot depth and open to

aquifers A through D, (2) 5.6 gpm per foot of drawdown when

at the 640-foot depth and open to aquifers A through G, and

(3) 76 5 gpm per foot of drawdown when at the full 750-foot

1

depth and open to all eight aquifers. The tests indicate

that most of the water available to the well is from the

deepest aquifer (zone H).

Borehole geophysical logging supplemented the drillers

log of the well and provided information on natural gamma

radiation, water temperature and resistivity, and borehole

diameter. In the completed well each aquifer zone is isolated

by cement seals, and piezometer pipes installed to zones B

through H allow a basis for defining the vertical hydraulic

gradient and ground-water movement in the area. The pipes

also permit chemical-quality monitoring of water in the

various aquifer zones. An additional pipe, installed for

providing thermistor access, allows recording of the geo-

thermal gradient in the well which provides a basis for

estimating vertical ground-water movement in the area.

2

INTRODUCTION

The test-observation well described in this report was

designed to yield key ground-water information for a highly

productive agricultural area of Washington, where ground

water is being used increasingly for irrigation. The data

already obtained from the construction and testing of the

well, and those expected in the future, are considered

essential to the sound management of the ground-water

resources of this area. Although some information on the

ground water was available from previous studies, much of

the knowledge being derived from this test-observation well

could not have been obtained in any other way. This study

will amplify and extend our understanding of the complex

ground-water-flow system of this area.

This study is part of an overall project designed for

drilling, testing, and periodically collecting data from

test-observation wells in selected areas of the State. The

wells are being drilled where there is a critical need for

ground-water data for water-management purposes, and where

the data cannot be obtained from existing wells or by other

reasonable means. This project is part of a continuing

cooperative program of water-resources investigations in

Washington, and is financed jointly by the U.S. Geological

3

Survey and the State of Washington Department of Ecology.

The data from this well will provide input to another current

cooperative investigation--the development of a mathematical

model, designed for analysis by use of a digital computer--of

the ground-water-flow system in east-central Washington and

of the relation between pumpage and decline of ground-water

levels.

The locations of this and other test-observation wells

drilled under this project during fiscal year 1971 are shown

in figure 1.

In basalt, most ground water occurs and moves in well-

defined permeable zones at or near the contacts between

individual basalt flows. These water-bearing zones (aquifers)

are separated from one another by the dense, nearly imperme-

able central parts of the flows. Hydraulic heads in the

individual aquifers, as reflected by water levels in wells

that tap them, usually vary with depth. In much of east-

central Washington the levels are highest in the shallow

basalt wells and lowest in the deeper wells.

Borehole geophysical logs and other data show that the

shallower aquifers in this area are being drained almost

continuously as a result of the short-circuiting effect of

leakage in uncased deep wells. The deep wells simply act as

4

124° 123° 22° 121° 120° nso 1:8° 117° -r A N A — -7-1)

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Davenport

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119°

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FIGURE 1.--Locations of test-observation wells in Washington.

open conduits in the basalt and interconnections between

otherwise isolated aquifers; the wells thereby allow down-

ward flow of ground water to deeper aquifers having lower

water levels.

In general, the downward leakage of ground water in an

uncased deep well, from aquifers at different depths and

with different hydraulic heads, results in a water level

that is a composite of the water levels of all aquifers in

hydraulic connection with the well. Table 1 presents the

effect of this composite water level in the test-observation

well at different depths during drilling. Virtually all

deep wells available and used for observation in east-

central Washington have such composite water levels. There-

fore, a comparison of the composite water levels from

various wells may be very misleading in an evaluation of

the relation between volume of pumpage and water-level declines

in a given area, Clearly, in view of the very serious degree

of ground-water depletion that is occurring in some parts

of the region, properly constructed test-observation wells

are essential to obtain the detailed information necessary for

a full understanding of the subsurface flow system and an

accurate determination and prediction of aquifer response.

6

TABLE 1.--Depth to water during drilling of Davenport test-observation well, September-October 1971

Date

Measurements in feet below land surface

Well depth Water level

Sept. 25 190 33

26 262 32.25

28 400 33.2

30 450 40.0

Oct. 1 520 34.5

2 560 33.7

5 588 33.8

12 614 137.2

14 664 156.2

15 750 160.4

7

Background and Ground-Water Problems of the Area

The test-observation well is located near Davenport,

Wash., in an area where the transition from dryland to

irrigated wheat farming has recently begun. Water levels in

the basalt-aquifer system are starting to decline locally.

The Davenport area is thought to be in the same stage of

ground-water development as that of the Odessa area to the

south (fig. 1) during the 1960's.

In the Odessa area, local areas of ground-water-level

decline were noticed in the early 1960's. By 1968 the declines

had increased and the areas of decline had coalesced and

covered about 700 square miles (Luzier and others, 1968) , and

by 1971 the area of decline had increased to more than 1,000

square miles. Widespread declines of water levels--but at

substantially lower annual rates--also have occurred in

shallow aquifers tapped by numerous domestic and stock wells.

Because these shallow wells normally are not much deeper

than the level of the water they tap, an annual decline of

only 1 or 2 feet may lower the water below the well bottoms,

causIng'much inconvenience and added expense to the owners.

8

RESULTS OF THE STUDY

Construction of the Well

The Davenport test-observation well was drilled by the

air-rotary method, and tested during the period September 23,

1970-May 14, 1971 by Adcock Drilling Co. of Lewiston, Idaho.

Table 2 provides the driller's log of the 750-foot well.

The well is cased to a depth of 75 feet and is open in

basalt the remaining depth.

Because water levels in wells that are open to all

aquifers penetrated are composites of the hydraulic heads

of all the aquifers, the well was designed to permit isola-

tion and individual measurement of water levels in the eight

aquifer zones penetrated. After final test pumping, 14-inch

pipes were suspended in the test hole, with short well screens

opposite each aquifer to be monitored. The hole then was back-

filled around the pipes with permeable gravel, and a cement

plug was placed at the base and top of each monitored zone

to isolate it; additional plugs were placed between these

major seals to prevent vertical circulation of water in the

well. The diagrammatic sketch of the well in figure 2 shows

aquifers A through H, the depths at which the cement plugs

and piezometer pipes are set and the water levels of each

aquifer just after installation, on September 8, 1971.

9

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TABLE 2.--Driller's log of well

Thick-ness DepthMaterial (feet) (feet)

Drilled by Adcock Drilling Co., Sept. 23, 1970-Mar. 17, 1971. Located 650 ft south and 1,200 ft west of the northeast corner of sec. 16, T. 24 N., R. 36 E. Altitude 2,372 ft msl. Casing 10 inches to 75 ft.

Silt 2 2

Basalt, cindery, and red clay, with trace of

Basalt, medium hard, slightly honeycombed, much

Basalt, broken and honeycombed, gray, with

Clay, brown, and soft brown basalt, in layers

Clay, soft, brown, and soft brown basalt, in

Basalt, medium hard, gray, streak of clay, tan

Basalt, hard, dark gray, drilled very rough, as if fractured from 184-190 ft, static water

Basalt, very hard, mixed light and dark gray,

(continued)

Clay, buff 2 4 Basalt, rotten 3 7 Basalt, solid, black, honeycombed 5 12 Basalt, solid, gray 12 24 Basalt, brown, weathered 10 34

water 7 41

green opallike material 5 46 Basalt, medium hard, gray 14 60 Basalt, medium soft, gray-green 10 70 Basalt, medium hard, gray 21 91 Basalt, soft, light gray 3 94 Material, bright green, opallike 2 96 Basalt, soft, gray 4 100

brown coating 31 131

about 1 ft thick 3 134 Basalt, medium soft, gray 2 136 Clay, very soft, tan-yellow 1 137

layers 1 to 2 ft thick 9 146

at155 ft--- 14 160 Basalt, medium hard, gray 14 174

level 33 ft---- 16 190

appears to be fractured, some water at 195 ft- 16 206

11

TABLE 2. --Driller's log of well--Continued

Thick-Material ness Depth

(feet) (feet)

Basalt, very hard, creviced at 213 ft, lost some water at about 216-218 ft in fractured rock 22 228

Basalt, hard, gray, with crevice at 229 ft and 247-250 ft 22 250

Basalt, hard, gray, some small creviced zones, static water level 32.25 ft 12 262

Basalt, gray, drilled a little faster than above 16 278

Basalt, very soft, broken, brown, may be water-bearing 3 281

Clay, black 2 283 Basalt, medium hard, black to dark gray,

slightly fractured 38 321 Clay, black 9 330 Clay, tan-brown 8 338 Clay, red 7 345 Clay, green 4 349 Basalt, fractured, gray, with some soft streaks

(clay?) 357-360 ft 11 360 Basalt, medium soft, dark gray 23 383 Basalt, medium hard, gray 17 400 Basalt, medium hard, gray, with some fractures at 403 and 420 ft 29 429

Basalt, honeycomb or decomposed, drilled fast 1 430 Basalt, medium hard, fractured, dark gray 4 434 Basalt, medium hard, dark gray 10 444 Basalt, medium hard, fractured, dark gray 4 448 Basalt, medium hard, dark gray 2 450 Basalt, medium soft, dark gray 11 461 Basalt, hard to medium hard, dark gray 4 465 Basalt, soft, fractured, lost some drilling

water 4 469 Basalt, medium hard, dark gray, fractured at

494 ft 41 510 Basalt, fractured, dark gray 3 513 Basalt, medium hard, dark gray, some fractures 529-532 ft 27 540

Basalt, very hard, fractured, dark gray 3 543 (continued)

12

TABLE 2.--Driller s log of well--Continued

Material

Basalt, very hard, dark gray, fractured at 572.5 and 577-582 ft 45 588

Basalt, very hard, dark gray Basalt, very hard, fractured, dark gray-----Cavity, water-yielding Basalt, fractured-----Clay Basalt, soft-Clay with some basalt or hard streaks Clay or basalt, soft Basalt, soft, fractured, dark gray Basalt, medium hard, fractured, dark gray Basalt, medium hard, dark gray Basalt, hard, dark gray Basalt, hard, fractured, dark gray Basalt, medium hard, dark gray Basalt, medium hard with soft streaks,

fractured

Basalt, soft, and dark clay -Basalt, medium hard, dark gray, with some

fractures-Basalt, soft, fractured, and some dark clay(? Basalt, medium hard, with some fractures Basalt, soft, fractured -Basalt, medium hard, dark gray, with some

Basalt, medium soft, dark gray, with some fractures

Basalt, medium hard, dark gray, with some fractures--

Basalt, hard, dark gray Basalt, medium hard, dark gray, with large

fractures Basalt, soft, and dark clay Basalt, medium hard, fractured

Thick-ness Depth

(feet) (feet)

11 599 4 603 2 605 1 606 3 609 2 611 3 614 1 615 2 617 13 630 16 646 6 652 4 656 8 664

6 670 6 676

4 680 6 686 6 692 3 695

5 700

12 712

13 725 5 730

3 733 5 738 12 750

13

Table 3 lists the actual water levels measured by steel

tape in each aquifer on that date.

Natural vertical movement or leakage of water from one

aquifer to another, through cracks and joint systems in the

dense rock, may have a warming or cooling effect on the

pattern of natural heat flow outward through the earth,

thereby causing a distortion in the geothermal gradient, By

careful measurement of this distortion, the rate of vertical

gr-Dund-water movement--and recharge of one aquifer by an

adjacent aquifer of higher head--may be calculated with

greater precision and at far less expense than by most other

methods available. For this purpose, a 11/4 -inch pipe (fig. 2)

was installed to the full depth of the hole to accommodate a

the rmistor (sensitive temperature-measuring device).

Pumping Tests

The Davenport well was test pumped during drilling, when

it had reached depths of 255, 640, and 750 feet (final depth).

The test at the 255-foot depth, with the well open to aquifers

A through D, used a rig-mounted bailer. At a rate of 26 gpm

(gallons per minute) for 6 hours, the drawdown was 5.4 feet,

indicating a specific capacity of 4.8 gpm per foot of drawdown.

TABLE 3.--Water levels of aquifer zones A through H, Sept. 8, 1971

Aquifer

A

B

C

D

F

G

H

Depth to water

(ft)

41.04

41.26

41.59

42.91

48.50

87.91

165.43

165.64

15

Utilizing a turbine pump for the testing at the 640-foot depth,

open to aquifers A through G, the well was pumped at 510 gpm

for 21 hours; the resultant drawdown of 90 feet indicated a

Specific capacity of about 5.7 gpm per foot. The final test

at the 750-foot depth--with the well open to aquifers A

through H--also utilized a turbine pump; at a rate of 536 gpm

for 21 hours, with a resultant drawdown of 6.8 feet, the

specific capacity was 78.8 gpm per foot. The tests indicate

that most of the water pumped from the well comes from the

aquifer zones below 640 feet.

Determinations of the transmissivity of the aquifer system

were attempted from both the drawdown and recovery data of

the final pumping test. In the absence of nearby wells to

serve as observation wells, estimates of transmissivity were

made by the graphical (straight-line) analysis of drawdown and

residual drawdown in the test well versus time (Jacob, 1950;

Theis, 1935). Recovery water levels during the test were

erratic and, therefore, not suitable for determination of

aquifer characteristics. However, the levels during pumping

were more regular, and the calculated value of transmissivity

was 40,000 square feet per day (300,000 gallons per day per

foot) for the drawdown part of the test.

16

Quality of Water

During each of the pump tests, samples of the water were

collected for chemical analysis. The results of these

analyses, shown in table 4, indicate that the water from all

the zones is of very good to excellent quality, suitable for

all common uses.

Geophysical Logs

Borehole geophysical logs were run on May 13, 1971, and

provided data on fluid temperature and resistivity, hole

diameter, and natural gamma radiation (fig. 3). In addition,

a flowmeter was used to determine the rate of vertical water

movement in the borehole.

The caliper log shows differences in the diameter of the

borehole; an increase in diameter indicates a soft or broken

zone in the basalt, which could be a source of water. The

trace of the caliper log (fig. 3) is reproduced approximately

in figure 2 to show its relation to the zones selected for

monitoring. Variations in hole diameter and in the character

of the rock materials also are reflected in the gamma log,

which is a measure of the small amount of natural gamma

radiation in the borehole.

17

TABLE 4. --Chemical analysis of water from aquifer zones A-D, A-F, and A-H

Values in milligrams per liter unless otherwise indicated

Item Well depth (ft)

255 640 750 (zones A-D) (zones A-F) (zones A-H)

Silica (SiO )240 45 55

Calcium (Ca) 23 12 12

Magnesium (Mg) 8.3 5.5 5.9

Sodium (Na) 12 29 31

Potassium (K) 2.7 3.9 3.6

Bicarbonate (HCO3) 102 128 142

Carbonate (CO )30 0 0

Sulfate (SO )415 9.0 9.5

Chloride (Cl) 8.2 3.9 3.5

Fluoride (F) .3 .8 .8

Nitrate (NO3)

8.6 .4 .3

Total dissolved solids 179 173 192

Hardness:

as CaCO 92 53 54 3

Nonca rbona te 8 0 0

Temperature (°C) 11 17.2 17.1

pH, in units 7.9 7.9 8.3

Specific conductance 246 231 238 (micromhos per centimeter at 25°C)

18

0 Increosing roaiotion

I I

Incrocsing resistance

I RESISTIVITY r)

LOG

CALIPER LOG

IN FEET BELOW LAND SURFACE

O

0-J

T E

MP

ER

AT

U R

E

1 I ! 10 12 A 16 18 20 22 24 50 54

INCHES TEMP°F

FIGURE 3. --Geophysical logs of the Davenport test-observation well.

19

The resistivity log shows the electrical resistivity of

the water in the borehole; because water with small amounts

of dissolved chemical constituents has a high electrical

resistance, the resistivity log is a rough indicator of

chemical quality of the water. The smooth, nearly vertical

trace of this resistivity log (fig. 3) shows that the chemical

quality of the ground water differs little from zone to zone

and also from top to bottom of the water column in the well.

This is confirmed by the chemical analyses (table 4) of water

samples taken when the well was at different depths.

The temperature log (fig. 3) shows a gradual increase in

water temperature from the static water level to a depth of

about 300 feet (near the top of aquifer zone E, fig. 2).

This temperature increase is a normal result of the heat flow

outward through the earth. However, the temperature log for

greater depths shows virtually no change and indicates that

there was an overall downward flow of water in the borehole

from zone E to the bottom. This downward flow was confirmed

by the flowmeter log (not shown) but the flow velocity was not

determined.

20

ADDITIONAL INFORMATION EXPECTED

The test-observation well is in a key location to monitor

the effects of irrigation pumpage in the Davenport area. In

addition to the information obtained on the sequence of

aquifers at the test site, the relative yields of various

zones, the geophysical profiles, and the general quality of

the ground water, the test-observation well is expected to

yield additional data, as summarized below.

1. Differences in the hydraulic head at the various depths

monitored by the piezometer pipes will define vertical

hydraulic gradients. These in turn will provide the

basis for meaningful estimates of the vertical move-

ment of water through the ground-water reservoir,

which are essential for a quantitative understanding

of the ground-water-flow system.

2. seasonal fluctuation of the water levels in the individual

piezometer pipes will clearly define the intensively

pumped aquifers, and should allow a better evaluation

of the vertical leakage from one aquifer to another.

Accurate temperature measurements through the thermistor3.

access pipe will assist in the interpretation of the

general pattern of ground-water flow, and also may

21

provide the basis for an independent method of estima-

ting vertical ground-water movement through the basalt

sequence.

4. The piezometer pipes are available to monitor any sizable

future changes in ground-water quality by means of

downhole conductivity sensors and, if necessary, by

withdrawal of water for chemical analysis.

In summary, the data already provided by the test-

observation well constitute valuable guidance for critical

water-management decisions that are needed for the area.

These data could not have been obtained by other practical

means. Additional data that are expected from the well may

prove to be even more helpful for management of the area's

valuable ground-water resource.

22

REFERENCES CITED

Jacob, C. E-, 1950, Flow of ground water, chap. 5, in Rouse,

Hunter, Engineering hydraulics: New York, John Wiley

& Sons.

Luzier, J. E., Bingham, J. W , Burt, R. J., and Barker, R. A.,

1968, Ground-water survey, Odessa-Lind area, Washington:

Washington Dept. Water Resources Water Supply Bull. 36,

31 p.

Theis, C. V., 1935, 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., pt. 2, p. 519-524.

23

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