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A Reevaluation of the Occurrence of 

Ground Water in the Nahiku Area, 

East Maui, Hawaii

Professional Paper 1618

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A Reevaluation of the Occurrence of 

Ground Water in the Nahiku Area, 

East Maui, Hawaii

By William Meyer

PROFESSIONAL PAPER 1618
U.S. DEPARTMENT OF THE INTERIOR

BRUCE BABBITT, Secretary

U.S. GEOLOGICAL SURVEY

Charles G. Groat, Director

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Library of Congress Cataloging-in-Publication Data

Meyer, William, 1939-

A reevaluation of the occurrence of ground water in the Nahiku area, East Maui, Hawaii 

/ by William Meyer.

p. cm. - (U.S. Geological Survey professional paper ; 1618) 

Includes bibliographical references. 

ISBN 0-607-9405 8-1 

1. Groundwater—Hawaii—Nahiku Region. I. Title. II. Series.

GB1025.H3M48 2000 

551.49'09969'21--dc21

00-037597
CONTENTS

Abstract.......................................................................................... 1

Introduction....................................................................................... 2

Description of the Study Area ................................................................... 2

Background.................................................................................. 2

Purpose and Scope ............................................................................ 7

Geologic Setting ................................................................................... 7

Stearns and Macdonald (1942) Conceptual Framework of Ground-Water Occurrence ............................. 8

Conceptual Framework for a Vertically Extensive Ground-Water Body ........................................ 14

Evidence for the Existence of the Stearns and Macdonald (1942) Concept of Ground-Water Occurrence .............. 14

Evidence for the Existence of a Vertically Extensive Ground-Water Body ...................................... 17

Hydraulic Conductivity and Ground-Water Levels ................................................... 18

Streamflow Characteristics...................................................................... 19

Water Levels in the Hana Volcanics ............................................................... 24

Ground-Water Level as a Function of Test-Hole Depth................................................ 24

Water Levels in the Kula Volcanics ............................................................... 34

Water Levels at Test-Hole Depths Near Sea Level.................................................... 38

Water Levels Outside the Artesian Water Body in the Honomanu Basalt.................................. 38

Ground-Water Movement Assuming a Vertically Extensive Ground-Water Body................................. 38

The Artesian Water Body ....................................................................... 40

The Convergence Zone and Source of Water to Big Spring............................................. 44

Vertical Thickness of the Fresh Ground-Water Lens. ....................................................... 46

Hydraulic Characteristics of the Rock Units .............................................................. 50

Summary and Conclusions ........................................................................... 52

References Cited ................................................................................... 54

Appendix A: Method of Water-Level Data Collection and Water Levels in Selected Test Holes ..................... 55

Method of Water-Level Data Collection............................................................ 55

Water Levels in Selected Test Holes............................................................... 57

Appendix B: General Considerations in the Use of the Water-Level Data ...................................... 61

Appendix C: Effect of Drilling on Water-Level Measurements ............................................... 62

Introduction of Drilling Fluid Under Pressure ....................................................... 62

Displacement of Water by the Drill Rod ........................................................... 64

Movement of Water in the Open Test Hole ......................................................... 65

Contents
Figures

1-3. Maps showing:

1. Hawaiian islands, island of Maui, and the study area......................................... 3

2. Test holes, Kuhiwa well, and springs, Nahiku area, Maui, Hawaii............................... 4

3. Ground-water areas on Maui, Hawaii, as defined by Stearns and Macdonald ...................... 6

4. Chart showing stratigraphic units and their water-bearing properties, Nahiku area, Maui, Hawaii ......... 9

5. Diagram illustrating the path of percolating and perched water in a lava terraine containing various types 

of interbedded perching structures typical of the Kula Volcanics (rocks are unsaturated in the absence 

of perched water)...................................................................... 10

6. Map showing geology; 1,100-foot and 800-foot artesian areas; and non-artesian areas according to

D.C. Cox, Nahiku area, Maui, Hawaii...................................................... 12

7. Sections showing water levels in open boreholes (A) in an area underlain by perched water bodies and 

a basal water body, and (B) in an area underlain by a vertically extensive water body where 

piezometric head declines vertically ....................................................... 13

8. Hydrograph showing water levels of various water bodies during drilling, Nahiku area, Maui, Hawaii ..... 15

9. Generalized section along line A-A' (fig. 16) showing ground-water movement within a vertically

extensive ground-water body............................................................. 16

10. Graph showing model-calculated water-table positions for simulations using various values of

horizontal hydraulic conductivity in an isotropic aquifer, Nahiku area, Maui, Hawaii ................ 19

11. Map showing stream-gaging stations, Nahiku area, Maui, Hawaii .................................. 20

12-14. Graphs showing:

12. Flow-duration curves of daily flows for selected streams, Koolau Ditch, and West Makapipi

Spring, Nahiku area, Maui, Hawaii..................................................... 22

13. Water level above the bottom of the test hole as a function of hole depth in the Hana Volcanics,

Nahiku area, Maui, Hawaii ........................................................... 27

14. Water levels in test holes compared with depth in the Hana Volcanics, Kula Volcanics, and

Honomanu Basalt, Nahiku area, Maui, Hawaii............................................ 28

15-16. Maps showing:

15. Water levels in test holes above the contact between the Hana and Kula Volcanics for testhole depths in the Kula Volcanics, Nahiku area, Maui, Hawaii................................ 30

16. First reported water levels in test holes, Kuhiwa well, and springs, Nahiku area, Maui, Hawaii........ 31

17-18. Graphs showing:

17. Morning water levels in selected test holes and Kuhiwa well, Nahiku area, Maui, Hawaii............ 32

18. Water level above the bottom of selected test holes as a function of hole depth, Nahiku area,

Maui, Hawaii ...................................................................... 35

19-20. Maps showing:

19. Water levels in test holes relative to the contact between the Hana and Kula Volcanics for

initial hole depth in the Honomanu Basalt, Nahiku area, Maui, Hawaii......................... 37

20. Water levels at hole depths near sea level, Nahiku area, Maui, Hawaii ........................... 39

21. Graph showing morning water levels and current-meter data indicating downward ground-water

movement in selected test holes, Nahiku area, Maui, Hawaii ................................... 40

22. Section showing test holes completed in the Honomanu Basalt and the altitude at which artesian

water was encountered at test holes 62, 74, 93, 94, and 99, Nahiku area, Maui, Hawaii ............... 41

23. Map showing potentiometric surface in the artesian water body, Nahiku area, Maui, Hawaii ............. 43

IV A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
24. Graph showing zone of converging ground-water movement and morning water levels in selected

test holes, Nahiku area, Maui, Hawaii ..................................................... 45

25-26. Maps showing:

25. Estimated altitude of the top of the convergence zone, Nahiku area, Maui, Hawaii.................. 47

26. Estimated altitude of the bottom of the convergence zone, Nahiku area, Maui, Hawaii .............. 48

27. Section showing convergence zone, zone of high permeability, and well logs in selected test holes

in the Nahiku area, Maui, Hawaii ......................................................... 49

28. Map showing calculated altitude of the freshwater-saltwater interface, Nahiku area, Maui, Hawaii ........ 51

Tables

1. Principal springs in the Nahiku area, Maui, Hawaii.................................................. 5

2. Selected flow characteristics at surface-water gaging stations in the Nahiku area, Maui, Hawaii .............. 21

3. Discharge at selected sites on Hanawi Stream, Maui, Hawaii.......................................... 23

4. Altitude, depth, and first reported water levels in test holes and Kuhiwa well in the Nahiku area,

Maui, Hawaii ............................................................................ 25

5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii............... 68

6. Water levels in selected test holes completed in Kula Volcanics, Nahiku area, Maui, Hawaii ................. 36

7. Altitude of the top and base of the zone of converging ground-water movement at selected test holes,

Nahiku area, Maui, Hawaii.................................................................. 42

8. Calculated altitude (in feet below sea level) of the midpoint of the transition zone between freshwater

and saltwater, Nahiku area, Maui, Hawaii...................................................... 50

Al. Water levels measured inside the drill rod with the bit at the bottom of the hole and using alternative methods

at selected hole depths in 12 test holes completed in the Honomanu Basalt, Nahiku area, Maui, Hawaii ..... 56

A2. Selected water-level measurements at test hole 90, Nahiku area, Maui, Hawaii............................ 58

A3. Selected water-level measurements at test hole 65, Nahiku area, Maui, Hawaii............................ 58

A4. Selected water-level measurements at test hole 87, Nahiku area, Maui, Hawaii............................ 59

A5. Selected water-level measurements at test hole 92, Nahiku area, Maui, Hawaii............................ 60

A6. Selected water-level measurements at test hole 85, Nahiku area, Maui, Hawaii............................ 60

A7. Depth-to-water measurements made inside the drill rod and inferred from current-meter measurements

at selected test holes, Nahiku area, Maui, Hawaii ................................................ 60

Cl. Depth to water in selected test holes for selected hole depths and times, Nahiku area, Maui, Hawaii........... 63

C2. Altitude of water level in selected test holes for selected times, Nahiku area, Maui, Hawaii.................. 65

C3. Estimated time, t, for water levels to decline to pre-drill-rod insertion values, following drill-rod insertion,

Nahiku area, Maui, Hawaii. ................................................................. 65

Contents V
Conversion Factors

Multiply By To obtain

acre 4,047 square meter

foot (ft) 0.3048 meter

foot per foot (ft/ft) 1 meter per meter

foot per day (ft/d) 0.3048 meter per day

cubic foot per second (ft3/s) 0.02832 cubic meter per second

inch (in.) 2.54 centimeter

mile (mi) 1.609 kilometer

square mile (mi ) 2.590 square kilometer

gallons per minute (gal/min) 3.785 liters per minute

million gallons per day (Mgal/d) 0.04381 cubic meters per second

VI A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
A Reevaluation of the Occurrence of Ground Water in 

the Nahiku Area, East Maui, Hawaii

By William Meyer

ABSTRACT

The Nahiku area is underlain by lavas of the 

Honomanu Basalt, Kula Volcanics, and Hana Volcanics. Stearns and Macdonald (H.T. Stearns and 

G.A. Macdonald, 1942, Geology and groundwater resources of the island of Maui, Hawaii: 

Hawaii Division of Hydrography Bulletin 7, 344 

p., 2 pis.) concluded that the ground-water system 

in the Nahiku area consists of a succession of 

perched water bodies in the Kula Volcanics, a 

perched artesian water body in the upper part of 

the Honomanu Basalt and a basal water body with 

water levels 5 to 10 feet above sea level in the 

Honomanu Basalt. These authors further concluded that streams in the area are perennial in 

areas where they intersect perched water bodies in 

the Kula Volcanics, but otherwise either lose water 

or are intermittent. The artesian water body was 

believed to be the source of water to Big Spring, 

the biggest spring on Maui.

Analysis of hydrologic data collected since 

the work of Stearns and Macdonald and a reevaluation of the data available to them indicates an 

alternative conclusion for the occurrence of 

ground water in the area; namely, that the groundwater system in the Nahiku area consists of a vertically extensive ground-water body extending 

from below sea level into the Hana Volcanics. 

Given a fully saturated ground-water body, the 

source of the head in the artesian water body is the 

water table in the Hana Volcanics. The source of 

water to Big Spring is a zone of relatively high permeability located, on average, about 220 feet 

above the artesian water body.

Corroboration for a vertically extensive 

ground-water body is provided by water-level data 

collected from 88 test holes drilled as part of a testdrilling program in the Nahiku area during the 

1930's and 1940's. These data indicate the presence of a significant amount of freshwater in the 

Hana Volcanics throughout the area. Stream gaging indicates the presence of perennial streamflow 

in streams underlain by these rocks. Also, discharge of ground water from springs in the Nahiku 

area is widespread, relatively large, and perennial 

in the Hana Volcanics.

The existence of a vertically extensive 

ground-water body is also confirmed by water levels measured in test holes completed at depths near 

sea level. Water levels in these test holes range 

from about 47 feet altitude near the shoreline to 

about 1,120 feet about 2 miles inland.

Evidence for the zone of high permeability 

located above the artesian water body is provided 

by water-level data and directional current-meter 

data collected in 10 of the test holes.

None of the test holes were dry as would be 

expected if the Hana Volcanics and the Honomanu 

Basalt outside of the artesian area and above the 

assumed basal aquifer were unsaturated. Instead 

water levels in many of the boreholes remained 

above the top of the Kula Volcanics as the holes 

were deepened into the Honomanu Basalt. The 

presence of water above the top of the Kula Volcanics is inconsistent with the mode of ground-water 

occurrence discussed by Stearns and Macdonald, 

but substantiates the concept of a vertically extensive water body extending from below sea level 

into the Hana Volcanics.

Abstract 1
INTRODUCTION

The Nahiku area (fig. 1) is underlain by gently 

sloping lava beds of the Honomanu Basalt, Kula Volcanics, and Hana Volcanics that emanated from the rift 

zones of Haleakala, a broad shield-shaped volcanic 

dome. The ground-water system in these lavas was 

originally described by Stearns and Macdonald (1942) 

who concluded that the area is underlain by a succession of perched water bodies in the Kula Volcanics and 

a perched artesian water body in the upper Honomanu 

Basalt. Stearns and Macdonald (1942) also concluded 

that a basal water body in the Honomanu Basalt underlies the entire area. This description is still the most 

commonly accepted interpretation of the occurrence of 

ground water in the area. A considerable amount of 

hydrologic data has been collected in the Nahiku area 

since the completion of the Stearns and Macdonald 

report, however, and methods and techniques of evaluating hydrologic data have improved substantially 

since the early 1940's. The new data and improved 

methods of analysis, combined with previously available data, lead to an alternative explanation for the 

occurrence of ground water in the area. Collectively, 

the information indicates that ground water in the 

Nahiku area occurs as a single, vertically extensive 

water body, extending from below sea level to altitudes 

as high as about 2,100 ft. The water body extends 

through all three rock units. The existence of this type 

of ground-water body (outside of a rift zone) has 

recently been identified in the Lihue area of Kauai 

(Izuka and Gingerich, 1998), but otherwise has not previously been reported in the State.

Description of the Study Area

The study area is in east Maui, Hawaii, near the 

town of Nahiku on the coast of the windward (northeastern) side of Haleakala (fig. 1). Maximum altitude 

of Haleakala is 10,023 ft. Median annual rainfall in the 

area ranges from a high of about 350 in. at altitudes 

between 2,000 and 4,000 ft (Giambelluca, 1986) to 

about 160 in. at the town of Nahiku.

The Nahiku area, as described in this report, 

encompasses an area centered near Hanawi Stream and 

extends just beyond Paakea Stream to the west and 

Kuhiwa Stream to the east (fig. 2). This area is mainly 

undeveloped forest land that covers a gently sloping 

land surface (10° to 14°) from Haleakala to the ocean. 

As stated by Takasaki and Yamanaga (1970), "the gentleness is mainly the result of lava flows which filled 

deeply eroded canyons and which later veneered most 

of the mountain." Despite the overall gentleness of 

slope in the area, the major streams west of Makapipi 

Stream have deeply eroded canyons and waterfalls, 

making much of the area relatively inaccessible. Precipitation occurs throughout the year, although 

extended dry periods of a month or more are common. 

Ground-water discharge from the area is high. Stearns 

and Macdonald (1942, p. 256-57,266-69, and plate 1) 

describe eight high-altitude springs with an aggregate 

average daily discharge of 14.26 Mgal/d (see table 1) 

and 17 high-altitude water-development tunnels constructed for agricultural purposes with an average 

aggregate discharge of 5.84 Mgal/d. As will be discussed in this report, a considerable amount of ground 

water also discharges at relatively high altitudes into 

streams in the area.

An irrigation ditch (Koolau Ditch) begins at East 

Branch Makapipi Stream and flows westward at an altitude of about 1,250 to 1,300 ft toward central Maui (fig. 

1). The principal streams crossed by the Koolau Ditch 

are perennial, and the ditch intercepts all of the dry 

weather flow of the streams from Makapipi Stream 

westward (Takasaki and Yamanaga, 1970, p. 14). 

Koolau Ditch itself also intercepts ground water.

Background

The general modes of occurrence of ground 

water in Hawaii have historically been divided into 

basal and high-level ground-water bodies. Basal 

ground water is characterized as a lens-shaped water 

body floating on and displacing saltwater. The altitude 

of the basal water table has previously been assumed to 

range from near sea level to a maximum altitude of 

about 30 ft.

High-level ground-water bodies are found at altitudes greater than that associated with basal ground 

water. High-level ground-water bodies have been 

assumed to result from either the impedance of the horizontal movement of ground water by dikes intruded 

into the lava flows, or from the impedance of the vertical movement of water by stratigraphic layers of low 

permeability. These low-permeability layers are usually described as ash beds, soil interbedded in lava 

flows, and as the dense interior of lava flows. Water 

above these layers is considered perched and the rock 

immediately below them is considered unsaturated. As 

commonly accepted, neither type of high-level groundA Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
160° 158°

22°

20°

Kauai

Niihau

Oahu

_____156°

I

HAWAII 

Molokai

c Lanai

Kahoolawe

Maui

°

Hawaii

INDEX MAP

156°20'

Nahiku

Hanawi 

drainage 

10,023 ft 

AA basin

156°

5 10 MILES

I_______l

0 5 10 KILOMETERS

Figure 1. Hawaiian islands, island of Maui, and the study area.

Introduction 3
20°50' 156°07' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area „ 

projection, standard parallels 20°39'30" and 20°57'30", u 

central meridian 156°20'15"

2,000

I

0

I 

500

4,000 FEET

1,000 METERS

EXPLANATION

1 « TEST HOLE AND NUMBER

Ilij SEDIMENTARY ROCKS

| HANA VOLCANICS

^ KULA VOLCANICS

HI HONOMANU BASALT

Pacific Ocean 

^

MAUI

Figure 2. Test holes, Kuhiwa well, and springs, Nahiku area, Maui, Hawaii (geology from Stearns and Macdonald, 1942).

4 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Table 1 . Principal springs in the Nahiku area, Maui, Hawaii

[Modified from Stearns and Macdonald, 1942, p. 256; Mgal/d, million gallons per day; —, none]

Spring1

22

23

24

25

--

-

--

29

Name

Ogino

Pali

Silveno

Kapaula

Big Spring

Hanawi 1

Hanawi 2

West Makapipi

Altitude 

(feet)

1,237

950

1,171

1,113

546

767

660

1,185

Location

Paakea Stream, between highway and Koolau Ditch

West Kapaula Stream, near junction with East Kapaula Stream

West Kapaula Stream, 150 ft north of highway

Kapaula Stream, just below highway

Hanawi Gulch, at 546 ft altitude

East wall of Hanawi Gulch, 2,500 ft northeast of highway bridge

East wall of Hanawi Gulch, 2,900 ft northeast of highway bridge

West Makapipi Stream, 450 ft north of Koolau Ditch

Total

Average 

discharge 

(Mgal/d)

0.20

20.5

0.18

0.44

10.4

1.17

0.88

0.49

14.26

Geologic unit

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Kula Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

1 Stearns and Macdonald, 1942, plate 1

2 Estimated November 1, 1939

water body is considered to be in contact with saltwater. Water levels in high-level water bodies may be 

several thousands of feet above sea level. A basal water 

body is generally considered to exist beneath perched 

water bodies.

A different mode of occurrence of high-level 

water on Hawaiian islands has been identified by Izuka 

and Gingerich (1998). Their work indicates that vertically extensive ground-water bodies can also form in 

lavas with relatively low values of hydraulic conductivity. The high-level water body described by Izuka 

and Gingerich (1998) is in direct contact with saltwater.

Stearns and Macdonald (1942, p. 19) described 

Haleakala as consisting "chiefly of thin-bedded lava 

flows dipping away from their respective summit vents 

and rift zones." And because of high rainfall in the 

Nahiku area, "all of the lavas are to some extent waterbearing, although some carry much more water than 

others" (Stearns and Macdonald, 1942, p. 255). These 

authors indicated that a basal water body with water 

levels 5 to 10 ft above sea level exists in areas of east 

Maui outside of the rift zones associated with Haleakala, including the Nahiku area (fig. 3). They also 

indicated that water bodies above the basal water body 

were perched and that perching structures were "intrusive rocks, ash beds, soil, and alluvium" (Stearns and 

Macdonald, 1942, p. 132). They described one of the 

perched water bodies as artesian and recognized that a 

similar system had not previously been described for 

any other location in the Hawaiian islands.

Interpretation of the occurrence of ground water 

by Stearns and Macdonald was, at least in part, based 

on geologic and water-level data collected during an 

extensive test-drilling program done in the 1930's and

1940's in the Nahiku area by the East Maui Irrigation 

Company (EMI) (fig. 2). The purpose of the drilling 

was to discover the source of the largest spring on 

Maui, Big Spring (fig. 2), which discharges into 

Hanawi Stream (Stearns and Macdonald, 1942, p. 225) 

and to determine the geologic control on the occurrence and movement of ground water in the Nahiku 

area (Takasaki and Yamanaga, 1970). Big Spring, at an 

altitude of 546 ft, was reported to have an average daily 

discharge of about 10.4 Mgal/d (Stearns and Macdonald, 1942, p. 212). The spring discharges from the 

base of a cliff at an altitude of only a few feet above the 

base-flow stage of Hanawi Stream. Stearns and Macdonald (1942) concluded that the source of water for 

Big Spring was the "perched" artesian water body.

A total of 100 test holes were drilled during the 

EMI test-drilling program, and in 1948 the Kuhiwa 

well was drilled ending the program (Takasaki and 

Yamanaga, 1970). Data from the first 86 test holes were 

available to Stearns and Macdonald. The final 14 holes 

were completed from 1942 to 1945 after publication of 

their report. Drilling extended from near Paakea 

Stream in the west to just past Kuhiwa Stream in the 

east, a distance of about 2 mi (fig. 2). From north to 

south, the area of test drilling extended inland from the 

ocean also for a distance of about 2 mi.

Stearns (in Stearns and Macdonald, 1942, 

p. 225-226) indicates that between December 1934 

and February 1942, the test drilling results provided 

"excellent records of interbedded soils and perched 

water tables." Stearns also indicates that artesian water 

was first encountered in 1941 while drilling test hole 85 

and that its discovery came as a surprise to the scientific 

workers in the area. On the basis of the artesian water

Introduction
156°40' 5 10 MILES

I_______l

— 5 —

EXPLANATION

BASAL WATER IN LAVAS

BASAL WATER IN SEDIMENTS

WATER CONFINED BY DIKES

WATER PERCHED ABOVE BASAL WATER

LINE OF EQUAL BASAL-WATER ALTITUDE 

Interval 5 feet. Datum is mean sea level. Dashed 

where inferred

Figure 3. Ground-water areas on Maui, Hawaii, as defined by Stearns and Macdonald (1942, plate 12).

6 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
level in the test hole, and the proximity of the test hole 

to Big Spring (fig. 2), Stearns concluded (Stearns and 

Macdonald, 1942, p. 225-226) that the artesian water 

body was the source of water to Big Spring. As stated 

by Stearns "In January 1941, while drilling a deep hole 

(no. 85) to locate supporting members that might perch 

Big Spring, Mr. Heizer encountered artesian water 395 

feet above sea level. The water was directly below the 

spring [altitude 546] in a permeable basalt between two 

dense lavas with sufficient head to rise through cracks 

to supply the spring." As further stated by Stearns 

(Stearns and Macdonald, 1942, p. 226), "The important 

lesson gained from the discovery of the source of Big 

Spring is the addition of the artesian hypothesis to studies of high-level springs issuing from stratified lavas in 

the Hawaiian islands."

As discussed herein, the artesian water body is 

not perched, rather it is part of a vertically extensive 

ground-water body with a water table in the Hana Volcanics. As also discussed, the source of water to Big 

Spring is not the artesian water body. Instead the source 

of water to Big Spring is a zone of high permeability 

located, on average, 220 ft above the artesian water 

body. Water converges toward the zone of high permeability from a large vertical distance both above and 

below the zone.

Purpose and Scope

The purpose of this report is to describe the reexamination of the occurrence of ground water in the 

Nahiku area. The report describes the conceptual 

framework and evidence for the occurrence of ground 

water as a series of perched water bodies underlain by 

a basal water body and it describes the occurrence of 

ground water as a vertically extensive ground-water 

body. The general movement of water within the vertically extensive water body and the source of water to 

Big Spring is also described.

The test holes drilled by EMI still are the only 

source of data on water levels as functions of depth for 

the area. Unpublished well logs from all the holes in the 

test-drilling program are on file at the USGS office in 

Honolulu. Test holes 87 through 100 penetrated to generally lower altitudes than the first 86 test holes. Even 

so, information on water levels near or below sea level 

is available from only five of the test holes and from 

Kuhiwa well.

Streamflow data is available for Waiaaka, 

Hanawi, and Makapipi Streams; Paakea and Kapaula

Gulches; and for several locations on the Koolau Ditch 

(see fig. 11). Data for these streams were examined in 

terms of base-flow and flow-duration characteristics. 

These data were supplemented with seepage measurements made on Hanawi Stream at selected time periods 

before and during this study. Ground-water recharge to 

the Hanawi Stream basin was calculated and evaluated 

against mean daily base flow estimated from streamflow data at two locations along the stream. The data 

permit an understanding of the rate of ground-water 

recharge and general direction of ground-water movement within the basin.

A water budget (Shade, 1999) was calculated for 

the Hanawi Stream basin as part of this study. This 

information was used in conjunction with the water 

levels measured during the test drilling program to calculate a value for the effective vertical hydraulic conductivity of the rocks in the Nahiku area. As part of this 

study also, Gingerich (1998) utilized the above information and the results of an aquifer test done at Kuhiwa 

well to construct a numerical ground-water model of 

the Hanawi Stream basin to investigate the relationship 

between ground-water levels and the hydraulic properties of the rocks in the basin.

GEOLOGIC SETTING

The lava flows of east Maui have been divided 

into the Honomanu Basalt, the Kula Volcanics, and the 

Hana Volcanics (Stearns and Macdonald, 1942; Langenheim and Clague, 1987). The Honomanu Basalt 

consists of pahoehoe and aa lava flows that range in 

thickness from 15 to 75 ft, although only a few exceed 

40ft.

The lavas of the Kula Volcanics cover the Honomanu Basalt to a thickness of "2,000 feet thick on the 

summit and 50 to 200 feet thick at the periphery," 

(Stearns and Macdonald, 1942, p. 7). Macdonald 

describes lava flows of the Kula Volcanics as "typically 

thick, dense, medium to light gray aa, sparingly vesicular to almost nonvesicular, with clinkery base and top 

and local streaks of clinker within the flow. The basal 

and upper clinkers are very persistent" (Stearns and 

Macdonald, 1942, p. 234). Macdonald gives values 

ranging from 50 to 80 ft for the thickness of individual 

lava flows within the Kula Volcanics.

Erosion during the final stages of emplacement 

of the Kula Volcanics formed deep canyons, and 

changes in sea level left thick alluvial deposits that 

extend high into the canyons. These deposits were later

Geologic Setting 7
covered by the Hana Volcanics. The lavas of the Hana 

Volcanics "followed valleys and swales, chiefly, leaving many of the interstream divides bare" (Stearns and 

Macdonald, 1942, p. 62). Lavas of the Hana Volcanics 

range in thickness from about 1 to perhaps 150 ft.

The general features of the geologic setting of 

the Nahiku area were described by Macdonald (Stearns 

and Macdonald, 1942, p. 229-233) as follows (the 

updated geologic names of Langenheim and Clague, 

1987, are in brackets):

The rocks of the Nahiku area are all volcanic, and by far the greater proportion are lava 

flows. Both aa and pahoehoe lavas are present, 

and range in composition from picritic basalts 

through basalts to basaltic andesites. Individual 

aa flows are generally thicker and in their central 

parts denser than the pahoehoe flows. Clinker 

forms moderately persistent layers at the tops and 

bases of aa flows, and in places forms irregular 

masses within the flows. Pyroclastic rocks are of 

little volumetric importance, but many of the intercalated soil layers, which perch ground water at 

high levels, are tuffaceous, containing fine ash 

drifted by the wind from fire fountains along the 

east rift zone. The quantity of ash would be 

greater were it not that the prevailing northeast 

winds blew such ash away from the Nahiku area. 

A single bed of lithic-vitric tuff is exposed in the 

sea cliff in the upper part of the Honomanu 

[Basalt].

The geologic history is one of a long succession of lava flows, covering surface drainage 

systems in various stages of evolution * * *. Many 

of the buried valleys support subterranean 

streams which move seaward through fractures 

and other apertures in the overlying lava. Stearns 

has divided the lava flows of East Maui into three 

groups—the Honomanu [Basalt], Kula [Volcanics], and Hana [Volcanics] (Part 1). In the Nahiku 

area the Honomanu [Basalt] lavas grade in petrographic character into the Kula [Volcanics] lavas, 

and the line of demarcation has been arbitrarily 

placed at the top of the transition zone at a surface marked by minor erosion. All the rocks in the 

Honomanu [Basalt] at Nahiku belong in the transition zone. The stratigraphic succession in the 

Nahiku area is shown in the table on page 230 

[figure 4, this report].

Intrusive rocks.—The only dike found in the 

area is exposed in the sea cliff 300 feet west of 

Kapaula Stream. The rock is a basaltic andesite, 

similar in petrographic character to several flows 

in the Hana and Kula [Volcanics]. It is dense and 

nonporphyritic, with prominent platy jointing parallel to the walls. It averages 4 feet thick and is 

essentially vertical, although in detail its course is 

somewhat sinuous. It cuts Honomanu Basalts in 

the lower part of the cliff, and passes upward into 

Kula lavas, where it is lost under a cover of soil 

and vegetation. Other dikes may be present, but 

have not been detected. They are certainly so few 

in number that they can have no important effect 

on the movement of ground water.

Geologic structure.—The structure of the 

area consists essentially of a series of irregular 

sheet and prisms of lava sloping toward the sea. 

Folding and important faulting are absent. Minor 

slickensides are present in several of the cores 

from the drill holes, but probably do not indicate 

any great amount of movement. They probably 

were caused by the slipping of blocks of lava during adjustments accompanying the compaction of 

the intercalated layers of loosely integrated clinker, caused by the weight of overlying rocks. No 

other evidence of faulting have been observed.

The stratigraphic succession in the Nahiku area 

is shown in figure 4 (modified from Stearns and Macdonald, 1942, p. 230-31), which also shows the 

descriptions by Stearns and Macdonald of the waterbearing properties of the various rocks within the stratigraphic columns.

STEARNS AND MACDONALD (1942) CONCEPTUAL FRAMEWORK OF GROUNDWATER OCCURRENCE

The conceptual framework of ground-water 

occurrence in the Nahiku area presented by Stearns and 

Macdonald (1942, fig. 13) is shown in figure 5. As 

shown, relatively small bodies of perched water are 

present in the Kula Volcanics, but for the most part this 

rock unit and the underlying Honomanu Basalt are 

unsaturated. The Hana Volcanics, which overlie the 

Kula Volcanics, are also assumed to be dry. The general 

movement of water is down the slope of the perching 

member and vertical where the perching member terminates. The "perched artesian water body" in the 

Honomanu Basalt identified by Stearns and Macdonald 

(1942) is shown in figure 5. The artesian water body is 

terminated some distance from the ocean by two joined 

aa lava flows. It is also of limited areal extent. Overlying streams would gain water from perched springs and 

seeps in and immediately above the Kula Volcanics, 

but otherwise the streams would lose water.

8 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Major stratigraphic unit 

(formation) Minor stratigraphic unit

Talus, landslide deposits, 

and beaches

Water-bearing properties

Highly permeable, but of too local extent to have any 

importance as water bearers. One spring issues from 

talus, but the water is probably derived from the base of 

the Kula lavas beneath the covering of talus.

LOCAL EROSIONAL UNCONFORMITY

Hana Volcanics

Hanawi flow

Paakea flow

Kuhiwa flow

Its small area makes it unimportant as a water bearer. A 

few small springs and seeps issue from the base of the 

flow.

Yields water from its basal part in several tunnels; 

several springs issue from it along Paakea Stream.

Yields water copiously in a water tunnel; also yields 

small amounts of water in two water tunnels and in 

several small springs along Makapipi Stream.

LOCAL EROSIONAL UNCONFORMITY

Mossman flow

Unimportant as a water bearer, although a number of 

seeps and small springs emerge from it at various 

localities, and small amounts of water issue from it in a 

water tunnel and in the main transportation tunnel of the 

Koolau Ditch.

LOCAL EROSIONAL UNCONFORMITY

Makaino flow

Kapaula flow

Yields water copiously in a water tunnel; Hanawi 

Springs 1 and 2, and other smaller springs also issue 

from this lava.

Yields water in three w ater tunnels and a number of small 

springs issue from it.

LOCAL EROSIONAL UNCONFORMITY

Waiaaka flow Nearly everywhere carries water, but the amount yielded 

at any single place is not large.

LOCAL EROSIONAL UNCONFORMITY

Makapipi flows Unimportant as water bearers, although several small 

springs and seeps emerge from them.

LOCAL EROSIONAL UNCONFORMITY

Big Falls flows

Several small springs emerge from these lavas in the sea 

cliff, at Big Falls on Hanawi Stream, and in the plunge 

pool at the mouth of Makaino Stream.

MAJOR EROSIONAL UNCONFORMITY

Kula Volcanics

Honomanu Basalt

The largest spring in the region, Big Spring on Hanawi 

Gulch, issues from the clinker phase of a Kula lava, and 

small springs emerge from Kula lavas at other localities.

Basal ground water is abundant; artesian water occurs in 

the upper, transitional lavas.

Figure 4. Stratigraphic units and their water-bearing properties, Nahiku area, Maui, Hawaii (modified from Stearns and 

Macdonald, 1942, p. 230-231).

Stearns and Macdonald (1942) Conceptual Framework of Gound-Water Occurance 9
Perched 

.spring

EXPLANATION

PERCOLATING WATER 

PERCHED WATER

PERCHING STRUCTURES

Ash or tuff

Weathered clinker

Dense aa

Soil

Poorly sorted gravel

Figure 5. Diagram illustrating the paths of percolating and perched water in a lava terraine containing various types of 

interbedded perching structures typical of the Kula Volcanics (rocks are unsaturated in the absence of perched water) 

(modified from Stearns and Macdonald, 1942, fig. 13).

10 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
The conceptual framework of Stearns and Macdonald (1942) is based largely on assumed permeability characteristics for the major rock units. The rocks of 

the Honomanu Basalt were considered highly permeable as a result of the presence of thin layers of clinker 

at the top and base of aa flows and the existence of 

"filled and abundant partly filled lava tubes in the 

pahoehoe. These openings, together with numerous 

vesicles and columnar and cross joints, make the rock 

exceedingly permeable" (Stearns and Macdonald, 

1942. p. 234). Stearns and Macdonald (1942, p. 72) 

report that, with the exception of a few small springs, 

only basal water had been found in the Honomanu 

Basalt. However, the existence of only basal water in 

the Honomanu Basalt is not supported by the data 

available from the Nahiku area. Presumably, Stearns 

and Macdonald were referring to other areas in central 

Maui where such data were available.

The artesian water body that Stearns and Macdonald (1942) identified and assumed to be perched in 

the Nahiku area is in the Honomanu Basalt, in rocks 

described as transitional between the Honomanu Basalt 

and the Kula Volcanics (Stearns and Macdonald, 

1942). Takasaki and Yamanaga (1970, p. 30-33), quoting from unpublished reports of D.C. Cox (1946 and 

1948), state that the water body was 50 to 200 ft thick 

and found in two separate areas. These areas, referred 

to as the 1,100 ft artesian area and the 800 ft artesian 

area together encompass about 300 acres (fig. 6). The 

1,100 ft area is defined by Kuhiwa well, test holes 99 

and 100. The 800 ft area is defined by test holes 85, 86, 

and 96.

Stearns and Macdonald (1942) considered the 

Kula Volcanics poorly permeable compared with the 

overlying Hana Volcanics and the underlying Honomanu Basalt although they state that the lavas of the 

Kula Volcanics are still "very permeable compared 

with most other rocks in the earth" (Stearns and Macdonald, 1942, p. 85). Big Spring issues from the basal 

clinker of a lava flow of the Kula Volcanics. Stearns 

and Macdonald (1942, p. 86), indicated that perched 

water in the Nahiku area occurs in the Kula Volcanics 

and results from the presence of "interstratified soils, 

vitric tuff beds, weathered clinker zones, and wide 

bands of dense rock" all within the Kula Volcanics. 

They also concluded that, for the most part, "individual 

lava beds of the Kula Volcanics are permeable and 

unable to perch water." Although the lavas of the Kula 

Volcanics were considered too permeable to perch 

water, Stearns and Macdonald observed that when

viewed as a unit, the Kula "contains enough more or 

less impermeable layers, even though discontinuous, to 

retard greatly the downward percolation of water in 

areas where 100 to 400 inches of rain falls annually 

[such as in the Nahiku area]. Thus, perennial streams, 

unusual features outside the dike complexes of the 

Hawaiian Islands, are found in the Kula rocks" (Stearns 

and Macdonald, 1942, p. 86). Finally, the assumed high 

permeability of the rocks of the Honomanu Basalt precluded perched water in these rocks and, with the 

exception of the perched artesian water body, only 

basal water is present.

The lavas of the Hana Volcanics were considered 

highly permeable by Stearns and Macdonald (1942, 

p. 7) who indicated that the high permeability of the 

Hana Volcanics and the general lack of interstratified 

perching beds within them allowed most of the rain to 

percolate to the Kula Volcanics. They further indicated 

that high infiltration rates in the Hana Volcanics precluded the presence of perennial streams where streams 

are underlain by these rocks (Stearns and Macdonald, 

1942, p. 102).

Water-level data that would support the conceptual framework in figure 5 would be test holes that were 

dry in the Hana Volcanics and the Kula Volcanics until 

a perched water body was penetrated (fig. 7A). Once 

the hole penetrated the perching layer, the only source 

of water, if any, in the hole would be from cascading 

water. Otherwise the hole would be dry until another 

perched water body was penetrated. Cascading water 

could cause water to be present in a hole but the amount 

of water would decrease as drilling progressed in the 

unsaturated rock. The water level would rise one time 

after the hole penetrated the perched artesian water 

body, but subsequently the depth of water in the hole 

would continue to decline and potentially the hole 

would become dry as the hole was deepened below the 

artesian zone. Depth to water in the borehole from cascading water would vary, but in general, less water 

would remain in the hole as a greater distance of permeable unsaturated rock was penetrated. Test holes in 

the Honomanu Basalt outside of the artesian water 

body would be expected to be dry or at least contain 

very little water at altitudes above the basal aquifer. 

Once the basal water body was penetrated, the water 

level in the hole would range from 5 to 10 ft above sea 

level. Presumably, the assumption by Stearns and Macdonald (1942) that basal water exists was based on the 

presence of springs near sea level, but this is not specifically discussed for the Nahiku area.

Stearns and Macdonald (1942) Conceptual Framework of Ground-Water Occurrence 11
20°50' 156°07' 156°06'

20°49' -

20°48' -

•j Non-artesian

A Hanawi Sprin

I Hanawi Sprin'

£, Artesian area

condition Big Spring 

unkrtQwn

•60V Kuhiwawell

CO J /S\

Base modified from U.S. Geological Survey 

digital data, 1:24,000, 1983, Albers equal area 

projection, standard parallels 20C39'30" and 20°5730", 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

I 

500 1,000 METERS

EXPLANATION

SEDIMENTARY ROCKS 51 « 

HANA VOLCANICS | 

KULA VOLCANICS B 

HONOMANU BASALT

TEST HOLE AND NUMBER 

800-FOOT ARTESIAN AREA 

1,100-FOOT ARTESIAN AREA

Figure 6. Geology; 1,100-foot and 800-foot artesian areas; and non-artesian areas according to D.C. Cox (//iTakasaki 

and Yamanaga, 1970 fig. 9), Nahiku area, Maui, Hawaii.

12 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
FEET 

1,800 -,

1,600 -

1,400 -

1,200 -

1,000 -

800 -

600 -

400 -

200 -

Sea level —

-200 -

-400

-600 -

-800 - 

-1,000

EXPLANATION

|——| UNSATURATED ROCK 

<=r> PERCHED WATER BODY

—— 800 —— LINE OF EQUAL HYDRAULIC HEADInterval, in feet, is variable

i—— - i—— FRESHWATER/SALTWATER INTERFACE 

_ _ 2. _ WATER TABLE

CASCADING WATER

OPEN BOREHOLE

Saltwater

FEET 

1,800 -i

1,600 -

1,400 —

1,200 -

1,000 -

800 -

600 -

400 -

200 -

Sea level —

-200 -

-400 -

-600 -

-800 - 

-1,000

Ocean

B

VERTICAL EXAGGERATION x4 2,000 4,000 FEET

0 500 1,000 METERS

Figure 7. Conceptual section showing water levels in open boreholes (A) in an area underlain by perched water 

bodies and a basal water body, and (B) in an area underlain by a vertically extensive water body where hydraulic 

head declines vertically.

Stearns and Macdonald (1942) Conceptual Framework of Ground-Water Occurrence 13
Given the conceptual framework of Stearns and 

Macdonald (1942), the first water encountered during 

test drilling, wherein water levels were relatively stable 

over some depth of the hole, has been interpreted as the 

first body of perched water underlying the area. Additional deeper bodies of perched water were identified at 

lower altitudes in test holes where water levels once 

again stabilized for some unspecified hole length (fig. 

8) (Takasaki and Yamanaga, 1970). The water levels 

illustrated in figure 8 also support the concept of a vertically extensive ground-water body.

CONCEPTUAL FRAMEWORK FOR A 

VERTICALLY EXTENSIVE GROUNDWATER BODY

Water-level data that would support a vertically 

extensive water body wherein the general movement of 

water is toward the ocean and vertically downward is 

depicted in figure IB and discussed below. Once the 

water table was penetrated in a borehole, water would 

be continually present as the hole was deepened. In a 

fully saturated ground-water flow system in which the 

vertical movement of water is generally downward, the 

altitude of the water level in the borehole would be 

expected to decrease as the borehole was deepened, but 

overall, the amount of water in the hole (defined herein 

as the height of the water above the bottom of the hole, 

tables 5 and 6) should increase as the hole is deepened. 

Given the geologic setting of the Nahiku area, the distribution of hydraulic conductivity would be expected 

to be inhomogenous and anisotropic. As a result it 

would be possible for relatively large declines in the 

altitude of the water level to occur in a given borehole 

at those horizons where relatively low values of vertical hydraulic conductivity were encountered or at horizons where the horizontal hydraulic conductivity is 

relatively high. Such declines could be misinterpreted 

as evidence of perched water.

The conceptual framework of ground-water 

occurrence in the Nahiku area assuming a vertically 

extensive ground-water body is shown in figure 9 

which depicts ground-water movement along section 

A-A' (see fig. 16). As shown, the rocks are saturated 

from below sea level to an altitude of at least 1,400 ft 

about 2 mi inland from the ocean. Depth of the water 

table averages about 50 ft below land surface. On the 

basis of the water-level data to be discussed herein, the 

water table is found in the Hana Volcanics where this 

rock is present. Altitude of the water table ranges from

about 47 ft near the ocean to about 1,400 ft 2 mi inland 

from the shoreline. Streamflow would be perennial 

where streams intersect the water table and would continue to gain water with decreasing altitude. Springs 

would occur wherever the land surface intersected permeable sections below the water table.

A principal feature within the section shown in 

figure 9 is the zone of convergence in which water is 

moving both downward and upward into the high permeability zone (see fig. 27) that is the source of water 

to Big Spring (not located in fig. 9). The zone is vertically extensive, averaging about 462 ft. The artesian 

water body is not depicted in the section in figure 9 but 

lies immediately below the bottom of the convergence 

zone. The artesian water body would be indicated by an 

increase in the altitude of the water level in the test hole 

once the artesian water body was penetrated (test holes 

93 and 99 in fig. 8).

The general movement of water is toward the 

ocean, streams, and major springs. The vertical movement of water would generally be downward, except in 

the area underlain by the artesian water body where 

upward flow from the latter body would occur. Upward 

flow would also begin at some point near the ocean.

Finally, as stated in the preceding section, 

Stearns and Macdonald (1942) assumed that the lava 

flows of the Hana and Kula Volcanics and the Honomanu Basalt were highly permeable in the Nahiku area. 

This assumption is significant and forms the conceptual 

basis for the relationship assumed by these authors 

among geology, ground-water occurrence, and streamflow. Although Stearns and Macdonald (1942) indicated that the volcanic rocks underlying the area are 

highly permeable, these authors had no quantitative 

data for the area for this conclusion. As will be discussed, a vertically extensive ground-water body 

requires that the horizontal hydraulic conductivity of 

the three rock units be significantly lower in the study 

area than the values normally assumed for volcanic 

rocks in the Hawaiian islands.

EVIDENCE FOR THE EXISTENCE OF THE 

STEARNS AND MACDONALD (1942) 

CONCEPT OF GROUND-WATER 

OCCURRENCE

Stearns and Macdonald (1942) did not specifically describe the evidence supporting their conceptual 

framework of ground-water occurrence in the Nahiku

14 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
1,400|W-»-4

1,300

1,200

1,100

1,000

900

800

700

600

^ 500

400

300

200

100

0

Perched water

Artesian perched water 

in Honomanu rocks

Test hole 99

(Land-surface

altitude 1,578 feet)

Test hole 93

(Land-surface

altitude 849 feet)

Artesian perched water 

in Honomanu rocks

Perched water

Test hole 89 

(Land-surface 

altitude 449 feet) Perched water

Test hole 88 Perched water

(Land-surface

altitude 135 feet)

Basal water in Honomanu rocks

J____I____I____I____I____l____I

1,400 1,300 1,200 1,100 1,000 900 800 700 600 500 400 300 200 100 0 

BOTTOM OF WELL, IN FEET RELATIVE TO MEAN SEA LEVEL

-100 -200 -300 -400

Figure 8. Hydrograph showing water levels of various water bodies during drilling, Nahiku area, Maui, Hawaii (from 

Takasaki and Yamanaga, 1970).

Evidence for the Existence of the Stearns and Macdonald (1942) Concept of Ground-Water Occurrence 15
A 1

-1.000

500

I I

1,000 METERS

__ _3Z. _ _

800-

EXPLANATION

TOP OF CONVERGENCE ZONE 

BOTTOM OF CONVERGENCE ZONE

APPROXIMATE POSITION OF FRESHWATER/SALTWATER 

INTERFACE

WATER TABLE

LINE OF EQUAL HYDRAULIC HEADInterval, in feet, is variable.

DIRECTION OF GROUND-WATER MOVEMENT

Figure 9. Generalized section along line yA-yA'(fig. 16) showing ground-water movement within a vertically 

extensive ground-water body. Vertical head loss based on water-level data at sea level (fig. 20).

16 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
area. Peterson (1981), however, states that the major 

features used to identify perched water bodies in the 

Hawaiian islands have been high-level springs. Presumably the high-level springs in the Nahiku area 

(table 1) would have formed some of the basis for 

Stearns and Macdonald's (1942) conceptual framework. In addition, Stearns and Macdonald had access 

to the water-level data from the first 86 test holes, and 

this data indicated that water levels in some of the test 

holes fell abruptly as they were deepened over a vertical distance of several feet or less, thus suggesting that 

a "perching layer" had been penetrated. These data, 

however, are not incompatible with the concept that 

ground-water occurs as a vertically extensive water 

body.

EVIDENCE FOR THE EXISTENCE OF A 

VERTICALLY EXTENSIVE GROUNDWATER BODY

Evidence indicating the existence of a vertically 

extensive ground-water body is summarized briefly 

here and is described in detail in the following sections.

An aquifer test in the upper 300 ft of the Honomanu Basalt (131 to 471 ft above sea level) at Kuhiwa 

well yielded a value for the horizontal hydraulic conductivity of the rock equal to 0.8 ft/d. This value is 

about three orders of magnitude lower than that normally assumed for the volcanic rocks of the Hawaiian 

islands. In contrast, Stearns and Macdonald (1942) had 

assumed highly permeable rocks in the Nahiku area.

In addition, although Stearns and Macdonald 

(1942) stated that streams overlying the Hana Volcanics are not perennial, the opposite is true. Streams 

underlain by Hana Volcanics become perennial at altitudes as high as 2,100 ft and continue to gain water 

from ground-water inflow with decreasing altitude. 

The existence of water in the Hana Volcanics is consistent with the presence of perennial streams where 

underlain by Hana Volcanics.

Water-level data obtained during the test-drilling 

program indicate the presence of a water table in the 

Hana Volcanics and a significant amount of freshwater 

in the Hana Volcanics throughout the study area. These 

results differ significantly with the conclusion of 

Stearns and Macdonald (1942) that the Hana Volcanics 

are unsaturated because of the high permeability of the 

rocks.

Water persisted in the test holes once encountered, and the amount of water tended to increase as

each hole was deepened. Twenty-three test holes penetrated into the Honomanu Basalt and five were sufficiently deep to have bottom hole altitudes near to or 

below sea level. On average, the amount of water at the 

completed depth of a given hole was 50 percent of the 

total length of the hole. The depth of the test holes 

ranged from 441 to 1,132 ft and averaged 718 ft. Water 

in Kuhiwa well, completed to 9 ft below sea level, 

stood 1,135 ft above the bottom of the well for a final 

hole depth of 1,405 ft. Once again, the conceptual 

model of Stearns and Macdonald (1942) would require 

that the test holes be dry or nearly so over a significant 

part of the rock each hole penetrated, and the water in 

Kuhiwa well would be expected to stand within 5 to 10 

ft of sea level.

The water level in many of the test holes 

remained above the top of the Kula Volcanics as the test 

holes were deepened through the Kula and remained 

above the Kula for significant distances into the Honomanu Basalt. However, if the Hana Volcanics were dry, 

and the Honomanu Basalt were dry outside of the artesian water body and above the assumed basal water 

body, as assumed by Stearns and Macdonald (1942), 

water would not be found above the top of the Kula 

Volcanics. For water levels to be in the Hana Volcanics, 

either (1) numerous perched water bodies would have 

to exist throughout the stratigraphic column from the 

Hana Volcanics to the bottom of the test holes in the 

Honomanu Basalt, and cascading water into the borehole would maintain a water level above the top of the 

Kula; or (2) the rocks would have to be saturated from 

the Hana Volcanics on down. Both of these conclusions 

present a different conceptual picture of ground-water 

occurrence than that of Stearns and Macdonald (1942). 

Given the general lack of interstratified perching beds 

in the Hana Volcanics and the Honomanu Basalt, the 

first interpretation is the least likely.

The general vertical movement of ground water 

in the study area is downward and the average vertical 

hydraulic gradient associated with this movement is 

0.47 ft/ft. Given this rate of head loss, it is not necessary for the water level in the test holes to remain above 

the top of Kula Volcanics as the test holes were deepened to conclude that the rocks are saturated below the 

first water encountered in the Hana Volcanics. The 

Kula Volcanics is relatively thick and an average vertical head loss of 0.47 ft/ft could easily result in the water 

levels falling below the top of the Kula with depth in 

many of the test holes even though the rocks are saturated. On the other hand, water level remained above

Evidence for the Existence of a Vertically Extensive Ground-Water Body 17
the Kula Volcanics in many of the holes as they were 

deepened into the Honomanu Basalt. This reinforces a 

conclusion that the rocks are saturated below a water 

table in the Hana Volcanics.

Water levels in the five test holes that penetrated 

to altitudes near to or below sea level did not indicate 

the existence of a basal water body with water levels 

between 5 to 10 ft as indicated by Stearns and Macdonald (1942). Rather, water levels ranged from about 

47 ft near the shoreline to 1,400 ft 2 mi inland.

Water levels in four of the five test holes 

described above were higher than the top of the Honomanu Basalt at their bottom hole altitudes near sea 

level. The water level in one of these test holes was still 

above the top of the Kula Volcanics. The water level in 

Kuhiwa well at its final bottom hole altitude of 9 ft 

below sea level was only 12 ft below the top of the Kula 

Volcanics. These data are inconsistent with the Stearns 

and Macdonald (1942) concept that the Honomanu 

Basalt is unsaturated and support the concept of a vertically extensive ground-water body.

Nine of the 23 test holes that were completed in 

the Honomanu Basalt were drilled at locations outside 

of the area of the "perched artesian aquifer" assumed 

by Stearns and Macdonald to exist in the Honomanu. 

The water levels in five of these test holes were above 

the top of the Kula Volcanics at their final bottom hole 

altitudes that ranged from 190 ft above sea level to 259 

ft below sea level. Water levels in 7 of the 9 holes were 

above the top of the Honomanu Basalt for bottom hole 

altitudes ranging from 260 to -340 ft. The water level 

in yet another remained above the top of the Honomanu 

Basalt to a bottom hole altitude of 99 ft below sea level. 

These data further reinforce the concept that the rocks 

of the Kula Volcanics and the Honomanu Basalt are 

saturated.

Geologic and hydrologic information were 

reported for 88 of the 100 test holes and water was 

reported in the each of those 88 holes. The Stearns and 

Macdonald (1942) concept would require holes completed in each of the three geologic units in the area to 

be dry.

Hydraulic Conductivity and GroundWater Levels

In general, volcanic rocks in Hawaii are considered uniformly highly permeable (Peterson, 1981, p. 

7). This concept is part of the underlying foundation for 

the current division of ground water in Hawaii into

basal and high-level water bodies. Values for hydraulic 

conductivity of the unweathered basaltic lava flows 

that make up the major basal aquifers in the State range 

from about 1,000 to 5,000 ft/d and average about 2,000 

ft/d (Mink and Lau, 1980, p. 7) and this approximate 

range of values is commonly assumed for all lava flows 

in the State. As a result, high-level water bodies are 

believed to form only from the impedance to horizontal 

ground-water movement by dikes or from the impedance to the vertical movement of ground water by 

stratigraphic zones of low permeability. In general, the 

high permeability assumed for the volcanic rocks probably results from the young age of the lava flows and, 

more importantly, from the thin vertical extent of individual lava flows (Peterson, 1981, p. 7). Average thickness of the permeable flows is less than 10 ft (Mink and 

Lau, 1980, p. 1).

In contrast, Izuka and Gingerich (1998) indicate 

that the regional hydraulic conductivity of the Koloa 

Volcanics in the southern Lihue Basin on the island of 

Kauai is probably less than 1 ft/d, about 3 orders of 

magnitude less permeable than the Mink and Lau 

(1980) average. The combination of low regional 

hydraulic conductivity and relatively high groundwater recharge results in a vertically extensive groundwater body with the water table reaching altitudes of 

several hundreds of feet above sea level.

Values of hydraulic conductivity for the underlying volcanic rocks are not known for many areas of the 

State, either because no tests have been done on existing wells or because no wells exist. Also, in some areas 

such as east Maui, individual lava flows are much 

thicker than those associated with the high-permeability flows. The thickness of lava flows in the Honomanu 

Basalt ranges from 15 to 75 ft, in the Kula Volcanics 

thickness ranges from 50 to 80 ft, and individual lava 

flows of the Hana Volcanics range from about 1 to 150 

ft.

The only data on the hydraulic conductivity of 

the rocks in the Nahiku area are from an aquifer test at 

the Kuhiwa well, which indicated that the horizontal 

hydraulic conductivity (AT/Z ) of the rocks penetrated by 

the well is 0.8 ft/d (unpub. aquifer-test archives, U.S. 

Geological Survey, Honolulu). This value is about 

three orders of magnitude lower than those values normally associated with Hawaiian basalts and of the same 

order of magnitude as reported by Izuka and Gingerich 

(1998) for the Koloa Volcanics in the southern Lihue 

Basin. As discussed in a later section of this report, the

18 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
> LU

LU

gCO

< 

tD

UJ

Q

^

p

8,000

7,000

6,000

5,000

4,000

3,000

2,000

1,000

0

Kh = 0.5 HORIZONTAL HYDRAULIC 

CONDUCTIVITY, IN FEET 

PER DAY

KE (effective vertical hydraulic conductivity) = Kh

0 5,000 10,000 15,000 20,000 25,000

DISTANCE, IN FEET

30,000 35,000 40,000

Figure 10. Model-calculated water-table positions for simulations using various values of horizontal hydraulic 

conductivity in an isotropic aquifer, Nahiku area, Maui, Hawaii. The shaded area represents the range in 

elevation where water is observed to discharge to the stream (modified from Gingerich, 1998).

upper bound for the effective vertical hydraulic conductivity (KE) of the rocks in the Nahiku area is 0.1 ft/d.

Gingerich (1998) constructed a numerical 

ground-water model of the Hanawi Stream basin to 

evaluate the relation between the position of the water 

table in the basin and the values of horizontal and vertical hydraulic conductivity of the aquifer.The model 

used ground-water recharge rates calculated for the 

basin as part of this study (Shade, 1999), a range of 

values for horizontal hydraulic conductivity consistent 

with the Kuhiwa well aquifer-test results (0.1 < KfT < 3 

ft/d), and a range of vertical hydraulic conductivity 

consistent with the calculation of this value discussed 

herein (0.005 < KE < 3.0 ft/d). The model predicted a 

range in the altitude of the water table from about 1,000 

to 6,000 ft (fig. 10). This result is significant in that it 

demonstrates that, incorporating data from two independent sources (a water-budget study, and an aquifer 

test) into a ground-water model that simulates saturated 

flow, results in model-predicted water levels in the 

range of those observed in the Nahiku area.

Streamflow Characteristics

Seven stream-gaging stations and two ditch- and 

one spring-gaging stations have been maintained by the 

USGS on the major streams between Paakea Gulch and 

Kuhiwa Stream (fig. 11) for various periods of time 

since 1923. Data on the altitude, period of record, and 

type of flow recorded at each of the gaging stations 

(perennial or intermittent) are given in table 2. As of 

1997, only two of these stations (5080 and 5090) were 

still operated by the USGS, both on Hanawi Stream 

(fig. 11).

Besides Hanawi Stream, stream gages were 

located on Kapaula and Paakea Gulches and on 

Makapipi and Waiaaka Streams. Five of the stations, 

including one of the two stations presently operating at 

Hanawi Stream (5090) were below the Koolau Ditch 

(fig. 11). Altitudes of these five stations ranged from 

500 to 920 ft (table 2), although the altitudes of four of 

the stations were within 500 to 650 ft. The other two 

stations, including the second stream gage still operating on Hanawi Stream (5080) are above the ditch.

Evidence for the Existence of a Vertically Extensive Ground-Water Body 19
20°50' 156°07' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000, 1983, Albers equal area 

projection, standard parallels 20°39'30" and 20°57'30", 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

500 1,000 METERS

EXPLANATION

SEDIMENTARY ROCKS 5090^ ACTIVE STREAM-GAGING STATION

AND ABBREVIATED NUMBER

HANA VOLCANICS 

KULA VOLCANICS

5060A INACTIVE DITCH-GAGING STATION 

AND ABBREVIATED NUMBER

INACTIVE STREAM-GAGING STATION 5065^ INACTIVE SPRING-GAGING STATION 

AND ABBREVIATED NUMBER AND ABBREVIATED NUMBER

HONOMANU BASALT 't6 1 • STREAMFLOW MEASUREMENT SITE

Figure 11. Stream-gaging stations, Nahiku area, Maui, Hawaii.

20 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Table 2. Selected flow characteristics at

[ft, feet; ft3/s, cubic feet per second; Q50 and Q90.

surface-water gaging stations in the Nahiku area, Maui, Hawaii

discharge equaled or exceeded 50 or 90 percent of the time]

Gaging 

station Name

Altitude 

(ft)

Q50 

(fWs)

Q90 

(tf/s)

Mean 

base flow

Type of flow Years operated Geologic unit

Stream-gaging station

5070 Makapipi Stream

5080 Upper Hanawi 

Stream

5090 Lower Hanawi

Stream

5 1 00 Upper Kapaula 

Gulch

5110 Lower Kapaula

920

1,318

500

1,346

540

2.40

6.97

21.0

5.20

2.40

0.00

2.70

16.6

1.50

2.00

3.4

6.1

20.1

4.0

2.8

Intermittent

Perennial

Perennial

Perennial

Perennial

1933^4

1923 to present

1933^6;

1993 to present

1923-62

1933^6

Hana Volcanics

Hana Volcanics

Kula Volcanics

Hana Volcanics

Kula Volcanics

Gulch

5130

5140

Waiaaka Stream

Paakea Gulch

650

650

0.82 0.57

3.8 3.0

0.8

3.9

Perennial

Perennial

1933^6

1933^6

Hana Volcanics

Hana Volcanics

Ditch- and spring-gaging station

5060

5065

5120

Koolau Ditch

West Makapipi 

Spring

Koolau Ditch

1,300

1,150

1,289

3.80 1.70

0.79 0.00

28.5 10.6

3.6

1.0

23.3

Perennial

Intermittent

Perennial

1949-65

1933-35; 

1937^3

1919-85

Hana Volcanics

Hana Volcanics

Hana Volcanics

Altitude of the gage currently operating on Hanawi 

Stream above Koolau Ditch is 1,318 ft. The second 

gaging station (5100) above the ditch was on Kapaula 

Gulch. Altitude of this gage was 1,346 ft. Five of the 

stations were on Hana Volcanics and the other two stations were on Kula Volcanics (fig. 11 and table 2).

Discharge measurements in the Koolau Ditch 

were made at gaging station 5120 from 1919 through 

1985 and at station 5060 from 1949 through 1965 (fig. 

11 and table 2). The ditch is in Hana Volcanics within 

the study area. Discharge also was measured at West 

Makapipi Spring (5065) from 1933 through 1935 and 

from 1937 through 1943. Flow from this spring is 

diverted into Koolau Ditch.

Flow-duration curves indicate that discharge at 

all of the stream-gaging stations was perennial with the 

exception of station 5070 on Makapipi Stream (fig. 12). 

Streamflow at this station was intermittent, although 

during some years, flow was continuous. Discharge in 

the Koolau Ditch at station 5120 underwent several 

periods of zero flow, which probably resulted from the 

diversion of water from the ditch for construction or 

repair purposes (Garrett Hew, East Maui Irrigation 

Company, oral commun., 1996); otherwise, discharge 

was continuous. Streamflow was perennial at the gaging stations on Hanawi Stream and Kapaula Gulch. 

Streamflow also was perennial at the gaging stations 

below Koolau Ditch on Waiaaka Stream and Paakea 

Gulch. Discharge at West Makapipi Spring was intermittent, although during some years discharge was 

continuous.

Because Koolau Ditch diverts all of the base 

flow of the streams above it, perennial Streamflow at 

gages below the ditch indicates that ground water discharges continuously at one or more locations between 

the ditch and the gage at each stream. Perennial streamflow at the gages above the ditch also indicates that 

ground water is discharging continuously at altitudes 

above these gages and at the ditch as well. Although 

rainfall is substantial above the ditch and the gages, 

drought can cause extended periods during which the 

streams and ditch would not flow without ground-water 

discharge.

The base-flow hydrograph for each gaging station was estimated using procedures proposed by the 

Institute of Hydrology (1980a, b), and although these 

procedures may not yield the true base flow, the subjectivity in manual methods is overcome and the results 

are indicative of the base flow (Wahl and Wahl, 1988). 

These hydrographs were used to calculate the mean 

base flow at each gage over their respective periods of 

record (table 2).

The cumulative mean annual discharge of 

ground water (base flow) at all the gaging stations is 

54.3 ft3/s (35.1 Mgal/d). This value includes an estimated value for mean annual ground-water discharge 

of 8.6 ft3/s into the Koolau Ditch above gage 5120, 

which is obtained by subtracting mean annual

Evidence for the Existence of a Vertically Extensive Ground-Water Body 21
O 

§ 

I

i

51

Koolau Ditch 

(ditch 5060)

West Makapipi Spring 

(spring 5065)

Makapipi Stream: 

(stream 5070) "

Upper Hanawi S

(stream 508

Upper Kapaula Stream 

(stream 5100)

Lower Kapaula Stream 

(stream 5110)

Koolau Ditch 

(ditch 5120)

Waiaaka S

(stream 5

51020305070809095 9999.999.99 0.010.1 1 51020305070809095 9999.999.99 0.010.1 1 51020305070809095 9999.999.99 0.010.1 1 51020305070809095 

PERCENT OF TIME INDICATED DISCHARGE WAS EQUALED OR EXCEEDED

Figure 12. Flow-duration curves of daily flows for selected streams, Koolau Ditch, and West Makapipi Spring, Nahiku area, M
ground-water discharge at upstream gages 5060,5065, 

5080, and 5100 from the mean annual ground-water 

discharge reported for 5120 in table 2. The cumulative 

mean annual discharge of ground-water from the Hana 

Volcanics is 31.4 ft3/s. Given that the mean annual discharge for these gages was estimated for different periods, some error is possible in the estimates of mean 

annual ground-water discharge at any location.

Ground-water discharge into Hanawi Stream 

below the ditch has been investigated by measuring 

instantaneous stream discharge simultaneously at 

selected sites. Simultaneous measurements were made 

at three locations below the Hana Highway at Hanawi 

Stream (sites 2, 3, and 4) on October 9,1974 (fig. 11 

and table 3). Measurements were repeated at these sites 

and one other site (site 1, fig. 11) during May 21-22, 

1975 (U.S. Geological Survey, 1976). These measurements were made at a time when discharge at site 2 

(station 5090) was below the discharge value equalled 

or exceeded 90 percent of the time (16.6 ft3/s, table 2), 

and below the value calculated for mean ground-water 

discharge.

The data in table 3 show that below Hana highway streamflow increased with decreasing altitude as a 

result of ground-water discharge into Hanawi Stream. 

About 15.4 ft3/s entered the stream between sites 1 and 

2. Big Spring and Hanawi 1 and 2 springs would have 

accounted for much, but not all of this discharge. The 

stream continues to gain from ground-water discharge 

below site 2. Flow of 3 to 4 ft3/s was gained between 

sites 2 and 3, and 1 to 3 ft3/s was gained between sites 

3 and 4. Total gain in streamflow from site 1 to site 4 

for May 21-22,1975 was 21.44 ft3/s. Because, as indicated by streamflow data at site 2, the seepage measurements were made at streamflow conditions during 

below-average ground-water discharge, the mean gain 

in streamflow from ground-water discharge between 

sites 1 and 4 would be somewhat greater than the rates 

estimated from the May 21-22, 1975 seepage run.

Hanawi Stream flows over Kula Volcanics for 

most of the reach between sites 1 and 3 (fig. 11). The 

stream flows over Hana and Kula Volcanics and Honomanu Basalt between sites 3 and 4, with the Honomanu 

Basalt being the predominant rock type. Big Spring 

issues from a basal clinker zone in the Kula Volcanics 

and Hanawi 1 and 2 springs issue from a lava flow in 

the Hana Volcanics (Stearns and Macdonald, 1942).

Seepage measurements on Hanawi Stream during July 26-28, 1994 indicated that ground-water discharge into the stream began at an altitude of about

Table 3. Discharge at selected sites on Hanawi Stream, 

Maui, Hawaii

[ft, feet; ft3/s, cubic feet per second; mi, mile; -, not measured. Datum 

from U.S. Geological Survey (1976)]

Measurements

Site 

(fig. 5)

1

2

3

4

Measured

previously 

(water years)

-

1927-32

1932-47

„

._

Date

5/21/75

10/9/74

5/22/75

10/9/74

5/22/75

10/9/74

5/21/75

Discharge 

(ft3/s)

0.56

14

16

18

19

19

22

Geologic unit

Hana Volcanics

Kula Volcanics

Hana Volcanics

Honomanu

Basalt

2,120 ft (R.A. Fontaine, U.S. Geological Survey, 

unpub. data, 1994). Flow below this altitude was continuous. At altitudes higher than this, several locations 

were found where ground water was discharging into 

the stream, but the discharge was small and the stream 

remained dry below these locations. These measurements were made following a period of dry weather 

when the source of water in the Hanawi Stream was 

ground water. The altitude at which ground-water discharge into the stream begins would be expected to 

vary seasonally.

In summary, because the lower gage on Hanawi 

Stream (5090) and the lower gage on Kapaula Gulch 

(5110) are on Kula Volcanics (fig. 11), perennial 

streamflow at these gages would be expected from 

either a perched or vertically extensive ground-water 

body. All of the other gages, however, are on Hana Volcanics (fig. 11). Perennial streamflow at these stations 

(excluding 5070) is not consistent with the conceptual 

model of the ground-water flow system of Steams and 

Macdonald (1942) but is consistent with the vertically 

extensive ground-water flow system concept.

The relatively high and perennial spring discharge at Hanawi 1 and 2 and the discharge of ground 

water into Koolau Ditch (all of which are on Hana Volcanics) are also inconsistent with a conceptual model 

that the Hana Volcanics is dry. Also inconsistent with 

the Steams and Macdonald concept is the fact that 

Hanawi Stream becomes perennial at an altitude of 

2,120 ft. This area also is immediately underlain by 

Hana Volcanics.

Evidence for the Existence of a Vertically Extensive Ground-Water Body 23
Water Levels in the Hana Volcanics

The study area is, for the most part, immediately 

underlain by Hana Volcanics (fig. 2). Sixty-six of the 

first 86 test holes were completed in the Hana Volcanics, although two of these holes (test holes 12 and 85) 

were later deepened into the Honomanu Basalt.

Water-level data were collected in 88 of the 100 

test holes drilled in the Nahiku area although the procedures for obtaining water-level measurements were not 

consistent. In nearly all of the deeper holes, water-level 

measurements were recorded each day as drilling progressed, while in some of the shallower holes water 

levels were reported only once for a single hole depth.

For the most part, water-level measurements 

were made through the center of the drill rod after the 

drill string was lowered to the bottom of the hole. The 

core bit usually was at the bottom of the hole or within 

a foot or so of the bottom when the water level was 

measured. Water levels so obtained should not be considered representative of the composite water level in 

the borehole assuming an open hole. Rather, as discussed in appendix A, the water level is probably an 

approximate measure of the composite head in the 

borehole for the interval below the drill rod, which in 

most cases would be the head at the bottom of the hole 

on the morning the measurement was made. Available 

data indicate that the composite water level for the 

entire borehole was actually higher than that recorded 

with the drill rod with the bit at the bottom of the hole. 

General considerations in the use of the water-level 

data are discussed in appendix B.

Altitude and depth of the test holes, the geologic 

unit in which each hole was completed, and the altitude 

at which water was first reported are shown in table 4. 

Most of the test holes were relatively shallow. Landsurface altitude of the test holes ranged from 1,845 to 

135 ft. Altitude of the bottom of the holes ranged from 

1,409 ft above sea level to 340 ft below sea level. The 

altitude of the first water level reported during drilling 

ranged from 1,468 to 47 ft.

The majority of the test holes completed in the 

Hana Volcanics were located above the Hana highway, 

in an area extending from west of Paakea Stream to east 

of Kuhiwa Stream (fig. 2). The average depth of these 

holes was about 70 ft, with the actual depths ranging 

from 10 to 204 ft. Ground-surface altitude of the test 

holes completed in the Hana Volcanics ranged from 

965 to 1,553 ft. Water-level data were reported for 43 

of these holes, although for some, water level was

reported only once during drilling. Depth below land 

surface to the first water reported ranged from 3 to 193 

ft and averaged 46 ft.

Data from test holes completed in the Hana Volcanics for which more than one water level was 

reported indicate that, once encountered, water 

remained in the holes and the amount of water in the 

hole generally increased as the hole was deepened (fig. 

13). In general, 50 ft or more of water was in the test 

holes at hole depths of about 100 ft in the Hana Volcanics. This is consistent with the vertically extensive 

flow system concept and inconsistent with the perched 

ground-water flow concept.

Water-level data from test holes that penetrated 

the Kula Volcanics or the Honomanu Basalt indicate 

the presence of a significant amount of freshwater in 

the Hana Volcanics throughout the study area because 

water levels in the test holes remained above the top of 

the Kula Volcanics for initial hole depths into the Kula 

(fig. 14). In general the height of the water level in the 

holes above the top of the Kula Volcanics for initial 

depths in the Kula ranged from 50 to 150 ft (fig. 15).

The configuration of the first water encountered 

in the Hana Volcanics is shown in figure 16. These 

water levels are assumed to represent the water table in 

the study area. The general slope of the water table is 

about 16 degrees toward the ocean. Altitude of the 

water table ranges from about 1,400 ft at the inland 

extent of the test drilling to about 47 ft near the shoreline at test hole 88. Ground water also discharges into 

the major streams, but detailed ground-water levels are 

not available to show this.

The test holes in the Nahiku area were drilled 

over a number of years and, as a result, there is the 

potential for error in the contour map. However, given 

that seasonal changes in water levels are probably not 

more than ten or several tens of feet, and that the area, 

with the exception of the ditch, is essentially unaffected 

by human development, the general characteristics of 

the movement of ground water indicated by the water 

levels in figure 16 should be accurate.

Ground-Water Level as a Function of TestHole Depth

Profiles of water levels compared with depth for 

the 23 test holes that penetrated the Honomanu Basalt 

indicate that, overall, water levels fell as the holes were 

deepened (fig. 17 and table 5, at end of report). These 

test holes (12,62,65,74, 81, 82, 83, 84, 85, 86, 87, 88,

24 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Table 4. Altitude, depth, and first reported water

[--, not measured or not applicable; datum is mean sea level.

levels in test holes and Kuhiwa well in the Nahiku area, Maui, Hawaii

Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Altitude

Test hole 

or well

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

Top 

(feet)

--

--

-

--

-

-

-

1,325

--

1,286

1,286

1,282

1,285

1,241

1,285

1,291

1,290

1,293

1,384

1,409

1,293

1,295

1,382

1,411

1,456

1,478

1,477

1,500

--

1,375

1,375

1,368

1,381

1,332

1,293

943

966

967

965

970

969

960

--

1,404

1,398?

1,395?

1,455

1,500

1,484

1,468

1,453

1,521

Bottom 

(feet)

--

--

~

~

--

-

--

1,259

-

1,230

1,192

345

1,166

1,213

1,192

1,228

1,213

1,128

1,257

1,265

1,176

1,166

1,259

1,241

1,345

1,376

1,394

1,409

--

1,248

1,305

1,295

1,296

1,222

1,070

574

820

838

895

552

791

773

-

1,297

1,385?

1,258

1,298

1,309

1,297

1,331

1,318

1,347

First reported water level

Hole depth 

(feet)

--

-

-

-

-

-

-

26

37

--

55

38

51

14

10

27

32

149

102

50

37

50

80

20

--

102

50

55

74

14

34

54

20

52

55

--

98

62

12

49

89

59

27

-

-

21

67

166

180

104

77

156

Depth to water 

(feet)

--

-

-

--

-

--

--

10

15

53

24

35

37

5

9

22

15

83

81

5

20

38

39

10

-

26

13

32

19

13

28

18

3

23

36

--

62

51

6

44

68

52

13

-

-

4

11

108

164

100

62

154

Water-level 

altitude (feet)

--

--

--

--

--

-

--

1,315

--

1,233

1,262

1,247

1,248

1,236

1,276

1,269

1,275

1,210

1,303

1,404

1,273

1,257

1,343

1,401

--

1,452

1,464

1,468

--

1,362

1,347

1,350

1,378

1,309

1,257

--

904

916

959

926

901

908

--

--

--

--

1,444

1,392

1,320

1,368

1,391

1,367

Geologic unit 

in which completed

--

--

-

-

--

--

--

Hana Volcanics

--

Hana Volcanics

Hana Volcanics

Honomanu Basalt

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

-

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Kula Volcanics

Kula Volcanics

Kula Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Honomanu Basalt

Kula Volcanics

Kula Volcanics

-

Hana Volcanics

-

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Evidence for the Existence of a Vertically Extensive Ground-Water Body 25
Table 4. Altitude, depth, and first reported water levels in test holes and Kuhiwa well in the Nahiku area, Maui, Hawaii-Continued

[--, not measured or not applicable; datum is mean sea level. Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Altitude

Test hole 

or well

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

100

Kuhiwa well

Top 

(feet)

1,472

1,483

1,553

1,470

1,295

1,294

1,388

1,403

1,454

1,395

1,329

1,470

1,066

Bottom 

(feet)

1,316

1,253

1,332

1,338

1,166

1,179

1,166

1,180

1,179

380

1,144

844

425

above Waiaka tunnel

above Waiaka tunnel

above Waiaka tunnel

above Waiaka tunnel

above Waiaka tunnel

above Waiaka tunnel

above Waiaka tunnel

First reported water level

Hole depth 

(feet)

145

204

148

126

50

51

57

46

35

60

42

55

18

52

46

76

41

30

32

47

Depth to water 

(feet)

136

193

138

123

43

45

34

35

23

37

39

50

15

40

36

70

31

22

29

44

Water-level 

altitude (feet)

1,336

1,290

1,415

1,347

1,252

1,249

1,354

1,368

1,431

1,358

1,290

1,420

1,051

-

-

-

~

-

-

-

Geologic unit 

in which completed

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Hana Volcanics

Kula Volcanics

Hana Volcanics

Honomanu Basalt

Hana Volcanics

Kula Volcanics

Honomanu Basalt

-

-

-

~

~

~

-

above Waiaka tunnel

1,072

1,073

1,076

1,089

1,107

1,124

1,103

984

924

945

977

1,003

1,494

465

135

449

864

762

902

849

796

780

785

826

1,015

1,578

1,845

1,396

440

823

860

809

807

824

830

463

446

155

536

12

677

-273

-340

-138

17

214

148

235

147

632

255

231

260

548

713

-9

131

54

73

83

55

122

72

177

71

170

65

45

496

194

166

137

181

184

131

155

352

--

284

192

140

184

596

954

83

38

29

35

46

65

43

10

61

106

36

44

323

90

88

109

131

106

81

105

189

-

87

129

91

174

449

260

989

1,035

1,047

1,054

1,061

1,059

1,060

974

863

839

941

959

1,171

375

47

340

733

656

821

744

607

-

698

697

924

1,404

1,396

1,135

Honomanu Basalt

Hana Volcanics

Hana Volcanics

Kula Volcanics

Kula Volcanics

Kula Volcanics

Kula Volcanics

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

Honomanu Basalt

26 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
160

120

80

40

0

160

120

80

40

Test hole 11 Test hole 13 Test hole 15 Test hole 16

i i i i

Test hole 17

I I I

Test hole 18

Test hole 20 Test hole 21 Test hole 22

i i i i r

Test hole 23

i i i i 

Test hole 24

i i i i 

Test hole 30

o

160

120

I I I I I I

Test hole 31 Test hole 32 Test hole 33 Test hole 37 Test hole 38

I I I

Test hole 39

O 

O

CQ 

UJ

O

CQ

80

40

120

I I I I I

i i i i r

Test hole 50 Test hole 51 Test hole 54

0 40 801201602002400 40 801201602002400 40 80120160200240

TEST HOLE DEPTH IN HANA VOLCANICS, IN FEET

~ 80

UJ 

UJ

DC 

UJ

I

40

0

160

I I I

Test hole 57 Test hole 58

120

80

40

160

0 40 80 1201602002400 40 80 120160200240

TEST HOLE LOCATIONS

0 40 80 120160200240

TEST HOLE DEPTH IN HANA VOLCANICS, IN FEET

Figure 13. Water level above the bottom of the test hole as a function of hole depth in the Hana Volcanics, Nahiku area, Maui, 

Hawaii.

Evidence for the Existence of a Vertically Extensive Ground-Water Body 27
C/D

g 

1

d

LL 

O

CL

O

LUtr 

tDLU

80 

60

40

20

0

( 

300

250 

200 

150

100

50 

0

Test hole 34

-

-

^""-^^^

-

) 25 50 75 0 5 10 15 20 25 3

. Test hole 77

-

-

-

-

-

) 25 50 75 0 5 10 15 20 25 3

250 

200

150

100

50

0 

0 C 

300

250 

200 

150

100

50

0 

0 C

. Test hole 35 

r++^s*-

-

-

-

-

i i i i i

) 25 50 75 0 5 10 15 20 25 3

. Test hole 78

a

^^**^*-,

-

-

*

-

-

25 50 75 0 5 10 15 20 25 3

125 

100

75

50

25

0 

0 C 

300

250 

200 

150

100

50

0 

0 (

. Test hole 41

-

-

-

-

-

-

) 25 50 75 0 5 10 15 20 25 3

. Test hole 79

-

i i i

-

-

) 25 50 75 0 5 10 15 20 25 3(

TEST HOLE TEST HOLE DEPTH TEST HOLE TEST HOLE DEPTH TEST HOLE TEST HOLE DEPTH 

PENETRATION IN IN KULA VOLCANICS, PENETRATION IN IN KULA VOLCANICS, PENETRATION IN IN KULA VOLCANICS 

HANA VOLCANICS, IN FEET HANA VOLCANICS, IN FEET HANA VOLCANICS, IN FEET 

IN PERCENT IN PERCENT IN PERCENT

•-v

EXPLANATION

WATER LEVEL-See appendix A 

for explanation of method

Inside drill rod with 

drill bit at bottom 

of hole

Current meter 

Raised drill bit

- n Raised pipe

TEST HOLE LOCATIONS

300

200

100

-700

I 150

100

50

0

-50

-100

-150

-200

-250

-400

0 25 50 75 0 25 50 75 0 110 220 330 0

200

Test hole 74

BaseofKu/a V

\

\ I *«•

olcanics M|

-300

25 50 75 0 25 50 75 0 200 400 600 0 25 50 75 0 25 50 75 0

200

30 60 90

100 - 

0

-100

-200 h

-300

I I I a_ 

Test hole 81

Base of Kula V

I • i • 4 —— * ——

olcanics

-*+->——

-

iii i i i i i i

0 25 50 75 0 25 50 75 0 60 120 180

TEST HOLE TEST HOLE TEST HOLE DEPTH

PENETRATION IN PENETRATION IN IN HONOMANU

HANA VOLCANICS, KULA VOLCANICS, BASALT, IN FEET

IN PERCENT IN PERCENT

100

0

--100

--200 

-300

Test hole 82!

Base of Kula Volcanics __ _ .

25 50 75 0 25 50 75 0 25 50 75~ "0 25 50 75 0 25 50 75 0 20 40 60

TEST HOLE TEST HOLE TEST HOLE DEPTH TEST HOLE TEST HOLE TEST HOLE DEPTH

PENETRATION IN PENETRATION IN IN HONOMANU PENETRATION IN PENETRATION IN IN HONOMANU

HANA VOLCANICS. KULA VOLCANICS. BASALT, IN FEET HANA VOLCANICS, KULA VOLCANICS, BASALT, IN FEET

IN PERCENT IN PERCENT IN PERCENT IN PERCENT

Figure 14. Water levels in test holes compared with depth in the Hana Volcanics, Kula Volcanics, and Honomanu Basalt, 

Nahiku area, Maui, Hawaii.

28 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
100 

0 

-100 

-200 

-300 

-400 

-500 

-finn

, i , | , i i 

. Test hole 83

* ———— M

Base of Kula V

i i i

V

olcanics

i i i

/

i

150 

100

50 

0 

-50 

-100 

-150 

-200

Testh'ole'84

" Base of Kula V

-* ——— 1»« m *

olcanics

-

-

100 

0 

-100 

-200 

-300 

-400 

-Rnn

- Test hole 85

- Base of Kula V

-

1

olcanics

^1-

1 -s

II-

; -

0 25 50 75 0 25 50 75 0 120 240 360 0 25 50 75 0 25 50 75 0 8 12 0 25 50 75 0 25 50 75 0 200 400 600

HEIGHT RELATIVE TOPVOLCANICS OF WATERLEVEL, FEET TOOFKULA IN

8

OOOOJOtil OO1OOOO O1OOOOC oooo c

" Base of Kula Volcanics *"

,,,.,,, ~T , V

-50 

-100 

-150 -_Base_of Kula\/ ojcanics__ _ _ 1 tJ —— -

D 25 50 75 0 25 50 75 0 90 180 270 0 25 50 75 0 25 50 75 0 120 240

i i i

. Test hole 89

"

- Base of Kula V

i i i

ill ' 4. '

olcanics

X 1 -

iM-^..

300

100 

0 

-100

Test hole 90 

%••*•

Base of Kula V

1

-

3(

1-

3 f" 

; -

olcanics

-

i i i i i i i i i i

D 25 50 75 0 25 50 75 0 100 200 300 0 25 50 75 0 25 50 75 0 100 200

. Test *\ 

hole 92 \ 

V

- Base of Kula V

-

*~--*1 •• —— 1»->

r- —V

olcanics <

I

100

0 

-100 

-200

Test hole 93 

Vt

Base of Kula V

—— vr —

<olcanics

3C

^

) 25 50 75 0 25 50 75 0 110 220 330 0 25 50 75 0 25 50 75 0 60 120

- Test hole 96 ' v*-»i- —— ' ' v, 200 

150

Test hole 97

**- —— —— if .

-

1E

-

-50 

-100

-150 

50 ( 

150

100 

50 

0 

-50 

-100 

-150

-200 

)0 ( 

150

100 

50 

0 

-50 

-100 

-150 

-200

-250 

0 ( 

200

100

Base of Kula V

3cp 

olcanics

U*

D 25 50 75 0 25 50 75 0 90 180 27

Test hole 91

Base of Kula V

<X»~'*"\^

olcanics

X .."

V

i i i i i i i i i i

D 25 50 75 0 25 50 75 0 60 120 1E

Test hole' 94

~_Base_gfKulaV

^

ojcanics__ _ _

AD 25 50 75 0 25 50 75 0 90 180 27

Test \ 

- hole 98 W 

•i

' ' '

•^

-

25 50 75 0 25 50 75 0 90 180 270 0 25 50 75 0 25 50 75 0 80 160 240

100

-600 -700 

0 25 50 75 0 25 50 75 0 120 240 360 0

TEST HOLE TEST HOLE TEST HOLE DEPTH 

PENETRATION IN PENETRATION IN IN HONOMANU 

HANA VOLCANICS. KULA VOLCANICS. BASALT, IN FEET 

IN PERCENT IN PERCENT

Kuhiwawell

-

-

Base of Kula V ojcanjcs^_ | _^

**\ i

i

•Stn

1

: ~

-500 

25 50 75 0 25 50 75 0 30 60 90 0 25 50 75 0 25 50 75 0 250 500 750

TEST HOLE TEST HOLE TEST HOLE DEPTH TEST HOLE TEST HOLE TEST HOLE DEPTH 

PENETRATION IN PENETRATION IN IN HONOMANU PENETRATION IN PENETRATION IN IN HONOMANU 

HANA VOLCANICS, KULA VOLCANICS. BASALT, IN FEET HANA VOLCANICS, KULA VOLCANICS, BASALT, IN FEET 

IN PERCENT IN PERCENT IN PERCENT IN PERCENT

Figure 14. Water levels in test holes compared with depth in the Hana Volcanics, Kula Volcanics, and Honomanu Basalt, 

Nahiku area, Maui,

Evidence for the Existence of a Vertically Extensive Ground-Water Body 29
20°50' 156°07' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area 

projection, standard parallels 20°39'30" and 20°57'30", 

central meridian 156°20'15"

2,000

I

r

500

4,000 FEET

I

T 

1,000 METERS

— 50 —

12 .

(41)*

EXPLANATION

LINE OF EQUAL WATER LEVEL-Interval 

100 feet

TEST HOLE AND NUMBER-Number in parentheses 

is initial water level in the Kula Volcanics, in feet 

above top of Kula Volcanics

Figure 15. Water levels above the contact between the Hana and Kula Volcanics for test-hole depths in the upper Kula 

Volcanics, Nahiku area, Maui, Hawaii.

30 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
156007' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area 

projection, standard parallels 20°39'30" and 20°57'30", 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

500 1,000 METERS

EXPLANATION

— 600 — LINE OF EQUAL WATER-LEVEL ALTITUDE-Interval 200 feet. 

Datum is mean sea level

A A'

I_____I LINE OF HYDROGEOLOGIC SECTION

TEST HOLE AND ALTITUDE OF FIRST REPORTED WATER LEVEL, 

IN FEET ABOVE MEAN SEA LEVEL

Figure 16. First reported watei levels in test holes, Kuhiwa well, and springs, Nahiku area, Maui, Hawaii.

Evidence for the Existence of a Vertically Extensive Ground-Water Body 31
(D

O

I(Da

o 3a

I

to

Iq 3

CQ

CD Q.g_ CD0) Q.cI

==0)

c

0)(B0)

ALTITUDE OF BOTTOM OF HOLE, IN FEET RELATIVE TO MEAN SEA LEVEL

O

DO
HI 

LJJ

LJJ 

2 

O

LJJ

LJJ

LJJ dX 

LL

O

2 

o

o

CD 

LL 

O 

LJJ 

Q

Test hole 93

m

400

300

200

Test hole 94 Test hole 96 Test hole 97

100'———I———I———!———I———I———y———X 2001———I———I———I———I———I———1-tSNXI 200 

200 400 600 800 1,0001,2001,400 0 200 400 600 800 1,0001,2001,400 0 200 400 600 800 1,0001,2001,400 0 200 400 600 800 1,0001,2001,400

Test hole 98

1,200 -

1,300

700

Test hole 100 Kuhiwa well

200 400 600 800 1,0001,2001,400 200 400 800 800 1,0001,2001,4001,800 200 400 600 800 1,0001,2001,4001,600 200 400 600 800 1,0001,2001,4001,600

MORNING WATER LEVEL, IN FEET ABOVE MEAN SEA LEVEL

EXPLANATION

WATER LEVEL-See appendix A 

for explanation of method

-——• Inside drill rod with drill bit at 

bottom of hole

- - - A Current meter

- - - V Raised drill bit

- - - n Raised pipe

| | HANAVOLCANICS 

F: : : : xl KULAVOLCANICS

HONOMANU BASALT

TEST HOLE LOCATIONS 

Figure 17. Morning water levels in selected test holes and Kuhiwa well, Nahiku area, Maui, Hawaii-Continued.

Evidence for the Existence of a Vertically Extensive Ground-Water Body 33
89, 90,91,92,93,94, 96,97,98,99,100, and Kuhiwa 

well) encompass the entire geographic area explored 

by the test-drilling program and include all of the test 

holes drilled to depths near to or below sea level (85, 

87,88, 89,90, and Kuhiwa well). Major rock units penetrated by a given test hole also are shown in table 5 

and figure 17.

The height of the water level above the bottom of 

the hole generally increased as each hole was deepened 

(fig. 18). Depth of the test holes ranged from 441 to 

1,132 ft and averaged 718 ft. The height of the water 

level above the bottom of the holes ranged from 81 to 

722 ft and averaged 350 ft. The height of the water 

level above the bottom of the hole in 14 of the 23 test 

holes equalled or exceeded 350 ft. With the exception 

of test hole 86 (where no water was recorded at a hole 

depth of 552 ft) and test hole 62 (which had only 3 ft of 

water at a bottom hole altitude of 770 ft), there was 

always water in each test hole as they were deepened 

(table 5). Water levels in test holes 86 and 62 are discussed further in appendix C.

The overall vertical hydraulic gradient (defined 

as the difference in the initial and final water level measured in the test hole divided by the hole length over 

which the difference in water levels was measured) in 

each of the deeper test holes is downward in all but two 

of the test holes (93 and 94, table 5). Downward gradients ranged from 0.03 to 0.97 ft/ft and averaged 0.47 ft/ 

ft. The vertical hydraulic gradient in Kuhiwa well was 

0.02 ft/ft. Artesian water was encountered in eight of 

the test holes (62, 74, 83, 92, 93, 94, 99, and 100; see 

fig. 14), but the overall hydraulic gradient in only two 

of these holes (93 and 94) was upward with gradients 

equal to -0.06 and -0.20 ft/ft, respectively.

Water Levels in the Kula Volcanics

Water levels in the Kula Volcanics are available 

from 29 test holes (fig. 14 and table 5). Six of these test 

holes, 34, 35, 41, 77, 78, and 79 (table 6) were completed at relatively shallow depths in the Kula Volcanics and the remaining 23 (table 5) were completed in 

the Honomanu Basalt. Water levels in the six test holes 

remained above the top of the Kula Volcanics for hole 

depths in the Kula.

Water levels in 11 of the 23 test holes completed 

in the Honomanu Basalt were above the top of the Kula 

Volcanics for all hole depths in the Kula Volcanics 

while water levels in another test hole, T-88, were a few 

feet above or below the contact. Once in the Honomanu

Basalt, the water level in this hole varied from 2 to 21 

ft above the Kula Volcanics for the first 100 ft into the 

Honomanu Basalt. Water levels in yet another test hole, 

74, were above the top of the Kula at depths where 

measurements were made, but these depths were all in 

the upper half of the Kula.

Water levels in the remaining 10 test holes ultimately fell below the top of the Kula Volcanics for hole 

depths in the Kula, although the water level in three of 

these holes rose back above the Kula Volcanics for hole 

depths in the Honomanu Basalt.

The 11 test holes wherein water levels remained 

above the top of the Kula as each hole was deepened 

through the Kula Volcanics were test holes 65, 81, 84, 

85, 87,89, 90,91,93,96, and 97 (fig. 14). Water levels 

in these holes also remained above the contact between 

the Hana and Kula Volcanics as each hole was initially 

deepened into the Honomanu Basalt. The water levels 

at the initial hole depth in the Honomanu Basalt ranged 

from 33 to 178 ft above the contact. The water level in 

one of these holes, test hole 85, remained above the 

contact between the Hana and Kula Volcanics for 

depths as much as 322 ft into the Honomanu Basalt. 

This hole depth corresponds to an altitude of 138 ft.

The ten test holes in which water levels ultimately fell below the top of the Kula Volcanics as drilling proceeded through the Kula were test holes 12, 62, 

82, 83, 86, 92, 94, 98, 99, and 100. Six of these holes 

(62, 83, 92, 94, 99, and 100) also encountered artesian 

water and two others (82 and 86) probably were completed at depths just above the artesian water body 

where water levels were still declining. Water levels in 

three (83, 92, and 94) of the six holes that encountered 

artesian water ultimately rose back above the top of the 

Kula for hole depths in the Honomanu Basalt, while the 

water level in test hole 62 rose to within about 50 ft of 

the top of the Kula.

The areal distribution of water levels in the 23 

test holes completed in the Honomanu Basalt relative 

to the altitude of the contact between the Hana and 

Kula Volcanics is shown in figure 19. The water levels 

indicated represent the measurement in the hole at the 

altitude nearest to the contact. The test holes in which 

the water level ultimately fell below the top of the Kula 

Volcanics are those farthest inland from the ocean.

34 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
LLJ 900

O

|_ 750

CO 

LJJ

i i i r

Test hole 12

i i i r 

Test hole 62 Test hole 65 Test hole 74 Test hole 81 Test hole 82 Test hole 83 

m

a

(D 

COi' 

o

O

Q.

I

OJ 

O

Q.

LJJ

I

i i i r

Test hole 86 Test hole 87

i i r i

Test hole 88 Test hole 89

n i r

Test hole 90 Test hole 91 Test hole 92 

i i i r

Test hole 96 Test hole 97 Test hole 98 Test hole 99

I ^^ I I I I «•» I I

Kuhiwa well f

0 300 600 900 1

•

i i i i

EXPLA

WATER L

append

explan

-—• Inside 

drill bi

of hole

- -A Curren

- -V Raised 

0 300 600 9001,2001,5000 300 600 9001,2001,5000 300 600 9001,2001,5000 300 600 9001,2001,5000 300 600 9001,2001,500 0 300 600 9001,2001,500 " " a Raised 

TEST HOLE DEPTH, IN FEET

Figure 18. Water level above the bottom of selected test holes as a function of hole depth, Nahiku area, Maui, Hawaii.
Table 6. Water levels in selected test holes completed in Kula Volcanics, Nahiku area, Maui, Hawaii

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics. Data from unpub. well logs in files at U.S. Geological Survey

o

a

<D

O 

o 

o

c

I

o

<D

O

3

a

<D

Land 

surface 

altitude

_._. Depth to top Depth to Vertical

death of Kula base of Kula hydraulic

p Volcanics Volcanics gradient

Hole 

depth

Bottom

hole 

altitude

Depth to 

water

Water

level

altitude

Water level 

above top

of Kula 

Volcanics

Rock 

unit1

Test hole 34

1,332 110 81 -- -- 52

77

103

110

1,280

1,255

1,229

1,222

23

24

50

48

1,309

1,308

1,282

1,284

58

57

31

33

Hana

Hana

Kula

Kula

Test hole 35

1,293 223 208 -- -- 55

88

108

145

186

223

1,238

1,205

1,185

1,148

1,107

1,070

36

29

29

46

30

17

1,257

1,264

1,264

1,247

1,263

1,276

172

179

179

162

178

191

Hana

Hana

Hana

Hana

Hana

Kula

Test hole 41

969 178 171 - - 89

122

176

880

847

793

68

67

69

901

902

900

103

104

102

Hana

Hana

Kula

Test hole 77

1,089 280 258 -- - 83

92

108

147

163

189

259

1,006

997

981

942

926

900

830

35

39

41

48

60

60

60

1,054

1,050

1,048

1,041

1,029

1,029

1,029

223

219

217

210

198

198

198

Hana

Hana

Hana

Hana

Hana

Hana

Kula

Test hole 78

1,107 300 287 - -- 55

59

84

101

115

135

138

167

283

288

1,052

1,048

1,023

1,006

992

972

969

940

824

819

46

55

55

53

53

54

54

54

73

73

1,061

1,052

1,052

1,054

1,054

1,053

1,053

1,053

1,034

1,034

241

232

232

234

234

233

233

233

214

214

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Kula

Test hole 79

1,124 300 280 - -- 62

122

150

182

200

271

293

1,062

1,002

974

942

924

853

831

—

65

66

66

66

83

83

—

1,059

1,058

1,058

1,058

1,041

1,041

—

215

214

214

214

197

197

—

Hana

Hana

Hana

Hana

Hana

Kula
20°50' 156°07' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area 

projection, standard parallels 20°39'30" and 20°57'30", 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

I 

500 1,000 METERS

EXPLANATION

12 . (-146)*

WATER LEVEL ABOVE TOP OF KULA 

VOLCANICS

WATER LEVEL BELOW TOP OF KULA 

VOLCANICS

BOUNDARY BETWEEN WATER LEVEL ABOVE AND 

BELOW TOP OF KULA VOLCANICS

TEST HOLE AND NUMBER-Number in parentheses 

is initial water level in the Honomanu Basalt, in feet 

relative to the top of the Kula Volcanics

Figure 19. Water levels in test holes relative to the contact between the Hana and Kula Volcanics for initial hole depth 

in the Honomanu Basalt, Nahiku area, Maui, Hawaii.

Evidence for the Existence of a Vertically Extensive Ground-Water Body 37
Water Levels at Test-Hole Depths Near 

Sea Level

Five test holes (85, 87, 88, 89, 90) and Kuhiwa 

well were drilled to depths near to or below sea level 

and water levels in these holes were examined to 

address the existence of a basal water body with water 

levels 5 to 10 ft above sea level (table 5, fig. 20). Except 

for Kuhiwa well, water levels shown in figure 20 were 

obtained from inside the drill rod with the bit at the bottom of the hole. These water levels are much higher 

than would be expected in a basal water body as 

defined by Stearns and Macdonald (1942). Water levels 

increase steeply from 47 ft at test hole 88 (a distance of 

about 300 ft from the ocean) to 1,126 ft at Kuhiwa well 

(about 2 mi inland from the ocean). These data support 

the framework for a vertically extensive ground-water 

system.

Water Levels Outside the Artesian Water 

Body in the Honomanu Basalt

Test holes 12, 87, 88, 89, 90, 91, 96, 97, and 98 

(see fig. 23) were drilled outside of the artesian water 

body and water levels in these holes were examined to 

understand ground-water occurrence in the Honomanu 

Basalt outside of the artesian body. In general, the presence of little or no water in these holes as they were 

deepened into the Honomanu Basalt would indicate 

that the rocks of the Honomanu Basalt are unsaturated 

in areas outside of the artesian water body and above 

the basal water body as defined by Stearns and Macdonald (1942). However, if water levels in the holes 

remained above the top of the Honomanu Basalt, the 

data would indicate that the rocks of the Honomanu 

Basalt are saturated, which is consistent with the concept of a vertically extensive water body.

Water levels in the test holes generally declined 

as each hole was deepened in the Honomanu Basalt, 

but even so, with the exception of test holes 12 and 89, 

the altitude of the water level in the holes remained 

above the top of the Honomanu Basalt (fig. 14 and table 

5).

The water level in test hole 89 was 44 ft below 

the top of the Honomanu Basalt at the final depth of the 

hole. However, the water level in test hole 89 remained 

above the top of the Honomanu Basalt to a borehole 

depth of 99 ft below sea level, indicating that the Honomanu is saturated at this location. The water level in

test hole 12 was 138 ft below the top of the Honomanu 

Basalt at the final bottom hole altitude of 345 ft.

The water level in three test holes (87, 88, and 

90) also remained above the top of the Kula Volcanics 

for bottom hole altitudes near to or below sea level 

(-259, -190, and 17 ft, respectively) and the water levels in two other holes (91 and 96) were still above the 

top of the Kula at their final bottom hole altitudes in the 

Honomanu Basalt of 163 and 119 ft, respectively (table 

5).

GROUND-WATER MOVEMENT ASSUMING 

A VERTICALLY EXTENSIVE GROUNDWATER BODY

The general movement of ground-water in the 

Nahiku area, assuming a vertically extensive groundwater body, is shown in figure 9. One of the major features shown is a water table that ranges from about 

1,400 ft 2 mi inland from the ocean to 47 ft near the 

shoreline. On the basis of the results of the test drilling, 

the water table is in the Hana Volcanics. The areal configuration of this surface (fig. 16) indicates a general 

movement of water toward the ocean. Another major 

feature shown in figure 9 is the presence of a convergence zone, so named because both water level and 

directional current-meter data collected during the test 

drilling program indicates that water is moving into 

this zone from above and below. The artesian water 

body is immediately below the convergence zone. Not 

shown in figure 9, but located in figure 27, is a layer of 

high permeability contained within the broader zone 

into which water is converging. The existence of this 

layer is indicated by directional current-meter data (figure 24) and it represents a horizon wherein the movement of ground water is predominately lateral. The 

altitude of the high permeability layer relative to Big 

Spring and the results of dye test experiment done during the test drilling indicate that the water moving 

within the layer is the source of water to Big Spring. 

Finally, the general decline of water levels as the test 

holes were deepened in the areas outside of the artesian 

water body indicates that the vertical movement of 

water is generally downward. Water levels and directional current-meter data collected in test holes 12 and 

87, which are outside the artesian water body, illustrate 

this movement (fig. 21).

Although the discussion in the preceding sections demonstrates that the Nahiku area is underlain by 

a vertically extensive water body, the following

38 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
20°50'

156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000, 1983, Albers equal area 

projection, standard parallels 20°39'30" and 20°57'30" 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

I I I 

500 1,000 METERS

EXPLANATION

— 600 — LINE OF EQUAL WATER-LEVEL ALTITUDE-Interval, 

in feet, is variable. Datum is mean seal level

85 • TEST HOLE AND NUMBER

50 WATER LEVEL, IN FEET ABOVE MEAN 

SEA LEVEL

Figure 20. Water levels at hole depths near sea level, Nahiku area, Maui, Hawaii.

Ground-Water Movement Assuming a Vertically Extensive Ground-Water Body 39
1,400

1,200

LLI 

W

O 

LLJ 1,000

5

LLJ

tj 8°° 

LU

LLJ

Q 600

I

LL

O

£ 400

O

CD

Test hole 12

I_____I_____I_____I

1

400

300

100

-100

-200

Test hole 87

1

1

I

200 I———————I———————1———————I———————I———————I INNNN1 .300

400 600 800 1,000 1,200 1,400 1,600 -200 0 200 400 600 800 1,000

MORNING WATER LEVEL, IN FEET ABOVE MEAN SEA LEVEL

- -- A

EXPLANATION

WATER LEVEL-See appendix A 

for explanation of method

Inside drill rod with 

drill bit at bottom 

of hole

Inferred from current-meter 

measurements

- - - V Raised drill bit

H^ HANAVOLCANICS

\:-<:-:\ KULA VOLCANICS

^^ HONOMANU BASALT

TEST HOLE LOCATIONS

Figure 21. Morning water levels and current-meter data indicating downward ground-water movement in selected test 

holes, Nahiku area, Maui, Hawaii.

sections describe the main features of the water body so 

that a complete picture of ground-water occurrence in 

the area is presented.

The Artesian Water Body

As indicated by water levels, only test holes 62, 

74, 83, 92, 93, 94, 99, and 100 intercepted artesian 

water at hole altitudes of 418,485,426,453, 373, 357, 

633, and 1,049 ft, respectively (table 5). These altitudes 

represent the altitude in the holes at which a rise in 

water levels began. The artesian water body was 

encountered in the Honomanu Basalt, except at test 

hole 100, where it is in the Kula Volcanics. Depth to the 

artesian water body in the Honomanu Basalt was 501, 

127, 72, 7, 36, 34, and 258 ft for test holes 62 through 

99, respectively (table 5). These data indicate that, 

toward the ocean, the position of the artesian water 

body in the Honomanu Basalt is generally higher in the 

stratigraphic column. A generalized geologic section 

showing selected test holes completed in the Honomanu Basalt; the altitude in test holes 62,74,83,92,93, 

94, 99, and 100 at which artesian water was first 

encountered; and the depth in each borehole at which 

water levels were last measured is shown in figure 22. 

Although, as discussed, Stearns and Macdonald 

(1942) as well as Cox (in Takasaki and Yamanaga, 

1970) (fig. 6) indicate that artesian water was encountered in test hole 85, this conclusion is not actually confirmed by water levels in the test hole (table 5). As 

discussed by Stearns (Stearns and Macdonald, 1942, 

p. 226), it was the apparent presence of artesian water 

in this hole that led to his conclusion that the artesian 

water body is the source of water for Big Spring. Their 

conclusion that test hole 85 intercepted artesian water 

may have been based on the results from directional 

current-meter data that were collected in the test hole 

during the test-drilling program. Current-meter data 

from test hole 85 indicate upward moving water 

between hole altitudes of 343 and 501 ft (table 7). Altitude of the water level in the hole over this interval 

ranged from 899 to 946 ft, respectively. That water levels increased in the same direction as the movement of

40 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
SOUTH EXPLANATION

I——I HANA VOLCANICS 

KULA VOLCANICS HONOMANU BASALT

DEPTH OF HOLE AT LAST 

WATER-LEVEL READING

ARTESIAN WATER 

ENCOUNTERED

LINE OF SECTION AND 

TEST HOLE LOCATIONS

03 W C/l -i-1 ? "7? -.. O5 ^° L_ 03 m Cfl »- -^ O 03 CT> |— l--i_ Q) f/> •" *~ ~r.

~~ '— —r— -~^^~ |_ 03 To -^ 2"o

_TM-«*«-—»——~-———

-100 -100

VERTICAL EXAGGERATION x4

Figure 22. Test holes completed in the Honomanu Basalt and the altitude at which artesian water was encountered at test holes 62, 74, 83, 92, 93, 94, 99, and 100, Nahiku area, Maui, Hawaii.
Table 7. Altitude of the top and base of the zone of converging ground-water movement at selected test holes, Nahiku 

area, Maui, Hawaii

[<, less than or equal to; —, not measured or not known; est, estimated]

Test 

hole

62

65

74

82

83

85

86

92

93

94

99

100

Altitude 

(feet)

Top

911

568

<750

667

715

1 803

1,314

'805

-

(est) 716

1,201

1,355

Base

380

-

440

-

370

*343

—

355

246

241

548

878

Thickness 

(feet)

531

—

310

—

345

460

—

450

•-

475

653

477

Directional current-meter data 

(altitude, in feet)

downward, 895 to 715; upward, 405 to 652

none

upward at 453 and 460; no other data

none

downward, 715 to 625 and 385 to 165; upward, 387 to 606

downward, 803 to 511; upward, 343 to 501

downward, 1,3 14 to 748

downward, 805(?) to 707; upward, 402 to 624

upward, 349 to 729

downward, 716 to 615; upward from 328 to 582; downward, 318 to 228

downward, 1,194 to 978; upward, 641 to 901

downward, 1,355 to 1,155; upward, 945 to 1,132

From current-meter data

water in test hole 85 indicates the possibility of an error 

in the water-level measurements or the current-meter 

data.

Cox (in Takasaki and Yamanaga, 1970) also 

included test hole 86 into those holes that penetrated 

the artesian water body (fig. 6) but water levels do not 

confirm this (table 5 and fig. 14), and directional 

current-meter data only indicate water moving downward (table 7). Cox may have included test hole 86 as 

one of the holes that penetrated artesian water because 

the water levels measured over the last 61 ft of the hole 

ranged from 873 to 880 ft in altitude (table 5) which is 

within the 800 ft artesian area defined by Cox (fig. 6). 

As will be discussed subsequently, the trend of waterlevel data in the hole may indicate that the test hole was 

completed just above the artesian water body.

Finally, a comparison of water levels in Kuhiwa 

well with those in nearby test hole 62 indicates that 

Kuhiwa well was completed in the artesian water body 

(table 5). Water-level measurements in Kuhiwa well, 

however, did not begin until the well had penetrated the 

artesian water body.

Test holes 65, 81, 82, 84, and 86 were all within 

the general area in which artesian water was encountered, but neither changes in water levels nor currentmeter data in these holes indicate artesian water (fig. 

14). On the basis of a projection between holes of the 

altitude at which artesian water was first encountered, 

these test holes probably were completed at depths too 

shallow to have intercepted the artesian water body, if 

present, or the last water-level measurements in the 

boreholes were made at depths too shallow to indicate

artesian water (fig. 22). For example, a comparison of 

water levels compared with depth in nearby test holes 

65 and 74, indicates that the water-level measurement 

in test hole 65 was made just above the altitude that 

water levels began to increase at test hole 74. Test hole 

82, which was near test hole 83, was completed at an 

altitude just above that in test hole 83 where the water 

level began to increase.

The Potentiometric Surface in the Artesian 

Water Body.—Figure 23 shows the potentiometric surface in the artesian water body, assuming that the water 

body is continuous throughout the area underlain by 

test holes 62, 74, 83, 92, 93, 94, 99, 100, and Kuhiwa 

well. The value of head selected was the highest artesian head in each test hole. As discussed and as shown 

in figure 6, previous work also assumed artesian water 

at test holes 85 and 86 and concluded that two separate 

artesian water bodies exist. The surface is dashed in the 

area of these two test holes to indicate the possibility of 

the latter conclusion. If a continuous water body is 

assumed (which is not fully supported by the data), 

artesian water levels decrease from an altitude of over 

1,100 ft at test holes 100, 99, 62, and Kuhiwa well to 

about 900 ft at test holes 85 and 86; to 800 ft at test 

holes 74, 83,92, and 93; and to about 700 ft at test hole 

94. The potentiometric surface slopes about 9 degrees 

toward Hanawi Stream.

Because an artesian water level was not encountered at test hole 85, the hydraulic head for this test hole 

(946 ft) represents the highest water level in the hole 

over the range in borehole altitude that upward moving 

water was indicated by the directional current-meter

42 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
20°50' 156°07'

20°49'

20°48'

156°06'

I

A nt\" 62 •/ Kuhiwa well

1 1U 71,120

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area 

projection, standard parallels 20°39'30" and 20°5r30", 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

500 1,000 METERS

EXPLANATION

— 600 - - LINE OF EQUAL POTENTIOMETRIC HEAD-Interval 100 feet. 

Datum is mean sea level. Dashed where uncertain

TEST HOLE AND NUMBER 

99 • In artesian area 

120 Outside artesian area 

1131 HYDRAULIC HEAD, IN FEET ABOVE MEAN SEA LEVEL

(273) INITIAL WATER LEVEL IN HANA VOLCANICS, IN FEET 

RELATIVE TO POTENTIOMETRIC WATER LEVEL

Figure 23. Potentiometric surface in the artesian water body, Nahiku area, Maui, Hawaii.

Ground-Water Movement Assuming a Vertically Extensive Ground-Water Body 43
data. The 880-ft head indicated for test hole 86 is the 

final measurement in the hole. If the artesian water 

body actually underlies this hole, the artesian head 

would be expected to be greater than this value given 

that water levels were not increasing substantially at 

the final hole depth.

Water levels measured within the artesian water 

body reached altitudes that were both above and below 

the top of the Kula Volcanics (fig. 14). The artesian 

water levels in test holes 62, 74, 99, and 100 were 

below the top of the Kula Volcanics with those in test 

hole 100 being the farthest below and those in test hole 

74 being the least. Artesian water levels in test holes 

83, 92, 93, 94, and Kuhiwa well were all above the top 

of the Kula Volcanics. Except at Kuhiwa well, this pattern of water levels represents a trend, in an oceanward 

direction, of increasing artesian head relative to the 

altitude of the top of the Kula Volcanics.

If the rocks are assumed to be saturated below a 

water table in the Hana Volcanics, the head in the Hana 

Volcanics would be higher than that in the artesian 

water body and the water table can be assumed to be 

the source of the head in the artesian water body. The 

difference between the uppermost or highest water 

level in the Hana Volcanics and the artesian head was 

calculated at most of the above test holes (fig. 23). 

Except at test hole 93, the water level in the Hana Volcanics exceeded the artesian head with the difference 

between the two generally decreasing in a downgradient direction. The uppermost water level in the Hana 

Volcanics was about 273 ft greater than the artesian 

head at test hole 99 and about 12 ft greater at test hole 

92. The artesian head at test hole 93 exceeds the head 

in the Hana Volcanics at this hole by 59 ft. Except for 

test hole 92, these results indicate that the water table 

in the Hana Volcanics is the source of head for the artesian water body. Because the water level in the Hana 

Volcanics is greater than the head in the artesian water 

body it is clear that the artesian water body cannot be 

the source of water to Big Spring.

The Convergence Zone and Source of 

Water to Big Spring

Water levels above the artesian water body 

exhibited two distinct patterns with regard to characteristics of water level compared with depth (fig. 14). The 

first pattern is best exemplified by test hole 62 and the 

second is characterized by test hole 100. Water levels at 

test hole 62 declined abruptly at about 300 ft above the

artesian water body after which water levels remained 

fairly constant with increasing hole depth until the artesian water body was encountered. Test holes 74, 83, 

and 92 exhibit this general pattern. Water levels at test 

hole 93 exhibit the pattern of relatively stable water 

levels immediately above the artesian water body. In 

contrast to this general pattern, water levels at test 

holes 99 and 100 declined abruptly before encountering the artesian water body after which water levels 

began to rise.

The pattern of water-level change compared 

with depth above the artesian water body exemplified 

by test hole 62 suggests a vertical zone above the artesian water body into which water is converging (see fig. 

9). Water would be moving downward into the zone 

from the area above the point where water levels begin 

to decrease abruptly and it would be moving upward 

into the zone from the artesian water body. Currentmeter data were collected over various intervals of the 

test holes that encountered artesian water and these 

data (table 7) combined with water levels plotted 

against depth in the boreholes illustrate this type of 

movement (fig. 24). The zone into which water is moving is relatively wide, ranging from 310 ft at test hole 

74 to 653 ft at test hole 99 (table 7). The top of the zone 

was selected as the altitude at which an abrupt decrease 

in water levels occurred or as the altitude at which current-meter data indicated downward flow of water. The 

bottom of the zone was selected as the altitude where 

an abrupt increase in water levels ceased to occur or as 

the altitude at which current-meter data indicated 

upward flow of water.

Water-levels in test holes 65 and 82 declined 

abruptly, with the decline occurring at about the altitude which would be expected if the zone into which 

water is converging underlies these two test holes (fig. 

22). Given this, values for the altitude of the top of the 

zone at these test holes are included in table 7. Test 

holes 65 and 82 were completed above the artesian 

water, assuming artesian water exists at these two locations.

Finally, water levels in test hole 85 fail to indicate the presence of artesian water whereas currentmeter data indicate the upward movement of water 

between the altitudes of 343 to 501 ft (fig. 14 and table 

7). Current-meter data also indicate downward movement between the altitudes of 803 to 511 ft (table 7). 

The altitudes of the top and bottom of the convergence 

zone indicated by the directional current-meter data at 

test hole 85 are roughly compatible with the top and

44 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
= 400

900 1,000 1,100 1,200 600

1,400

1,000

UUi————i————i————i————i————i—c^^j 100 

400 500 600 700 800 900 1,000 200 300 400 500 600 700 800 900 1,000 600

9001—————|—————i—————|—————|——r^—, 800

800 1,000 1,200 1,400

800

700

600

500

400

300

200

I I I Test hole 92

«r^

Si

_ I 

• ^- -------- —— <

1

' J

j

}

:

^ / _•

- \

:£T

«

1

Test hole 94

.-A m

550 600 650 700 750 800

MORNING WATER LEVEL,

IN FEET ABOVE 

MEAN SEA LEVEL

800 1,000 1,200 1,400

700

1,600 800 1,000 1,200 1,400 1,600

MORNING WATER LEVEL, IN FEET ABOVE MEAN SEA LEVEL

EXPLANATION

ZONE OF CONVERGING GROUND-WATER 

MOVEMENT-Dashed where uncertain

DIRECTION OF WATER MOVEMENT 

BASED ON CURRENT-METER DATA

WATER LEVEL INSIDE DRILL ROD 

WITH DRILL BIT AT BOTTOM 

OF HOLE

WATER LEVEL-See appendix A 

for explanation of method

• - - A Inferred from current-meter 

measurements

• - D Raised drill bit

• - - v Raised pipe

TEST HOLE LOCATIONS

HANA VOLCANICS 

[:?xl KULA VOLCANICS 

^^ HONOMANU BASALT

Figure 24. Zone of converging ground-water movement and morning water levels in selected test holes, Nahiku area, 

Maui, Hawaii.

Ground-Water Movement Assuming a Vertically Extensive Ground-Water Body 45
bottom of the convergence zone indicated at test hole 

83.

The estimated altitudes of the top and base of the 

zone into which water is converging above the artesian 

water body are shown in figures 25 and 26, respectively, and are also provided in table 7. Not all of the 

test holes completely penetrated the zone and, as a 

result, the bottom of the convergence zone could not be 

determined at these holes. The zone, if continuous, 

slopes downward toward the ocean at about 10 degrees. 

The altitude of the top of the zone ranges from 1,355 ft 

at test hole 100 to 568 ft at test hole 65.

A transect through test holes 100,99,62,74, 85, 

83, 92, 93, and 94 indicates that the convergence zone 

lies wholly within the Kula Volcanics at test hole 100, 

extends from the Kula Volcanics into the Honomanu 

Basalt at test hole 99, and is almost wholly within the 

Honomanu Basalt at test hole 62 (fig. 27). Further 

downslope it extends from the lower half of the Kula 

Volcanics to the upper part of the Honomanu Basalt at 

test hole 74. At test hole 83 the convergence zone 

extends from the upper two-thirds of the Kula Volcanics to the upper Honomanu Basalt. At test holes 92 

and 94, the zone extends from the Hana Volcanics into 

the Honomanu Basalt. On the basis of current-meter 

data alone, the downward movement of water at test 

hole 85 begins several feet above the bottom of the 

Hana Volcanics while the upward movement begins in 

the Honomanu Basalt.

The current-meter data in seven of the holes also 

indicate the existence of a narrow zone (zone of high 

permeability, fig. 27) in which the upward and downward movement of water was not detected and the lateral movement of water presumably dominates. The 

convergence of water into this narrow zone suggests 

that the permeability of the zone is relatively high. The 

thickness of the high permeability zone ranges from 10 

ft at test hole 85 to 103 ft at test hole 92. The zone of 

high permeability is contained within the Kula Volcanics at all of the test holes except test hole 62, where it 

is in the Honomanu Basalt.

Given that the general lateral movement of water 

in the area is toward the major discharge areas, such as 

streams, springs, and the ocean, the lateral movement 

of water in the convergence zone probably conforms to 

this movement. One of the consequences of this movement would be that areas of significant ground-water 

discharge into Hanawi Stream should occur within the 

area defined by the intersection of the stream and the 

convergence zone. The zone of high permeability in the

test holes where the horizontal movement of water predominates would be expected to represent an area of 

relatively significant ground-water discharge even 

within the larger convergence zone.

Ground-water discharge into Hanawi Stream 

increases with descending altitude, and seepage data 

indicate that most ground water discharges where the 

stream has eroded onto Kula Volcanics, beginning in 

the area of Big Spring and extending to the ocean. 

From Big Spring to site 3 (fig. 11), Hanawi Stream 

overlies Kula Volcanics, while from site 3 to site 4 (fig. 

11) the stream mainly flows on Honomanu Basalt, 

although Hana and Kula Volcanics are present. This 

area of ground-water discharge is consistent with the 

analysis in the preceding paragraphs that indicates the 

convergence zone lies within the Kula Volcanics and 

the upper part of the Honomanu Basalt. Even more significantly, the altitude of the zone of high permeability 

at test hole 83 (625 to 606 ft) which is near Big Spring 

and the altitude of Big Spring (546 ft) (fig. 27) strongly 

suggest that water moving in the zone of high permeability is the source of water for Big Spring.

Further support for the relation between the convergence zone and ground-water discharge to Hanawi 

Stream is available from dye experiments done at test 

holes 82, 83, and 92 during the test-drilling program. 

Dye was injected into these holes at altitudes of 576, 

554, and 489 ft, respectively, and appeared in Big 

Spring several hours later. The injection of the dye at 

test holes 83 and 92 was in the range of altitude where 

water is moving upward toward the zone of high permeability.

VERTICAL THICKNESS OF THE FRESH 

GROUND-WATER LENS

The water table increases from an altitude of 

about 47 ft in the vicinity of test hole 88 to about 1,400 

ft in the vicinity of test hole 99 (fig. 16). On the basis 

of the results of the seepage measurements on Hanawi 

Stream, the height of the water table can be expected to 

increase inland from this point to at least 2,100 ft in 

altitude.

In general, water-table altitudes of the magnitude 

of those discussed above would be assumed to imply 

that the thickness of freshwater below sea level is relatively large, assuming that the depth to the freshwatersaltwater interface can reasonably be approximated by 

the Ghyben-Herzberg relation. Izuka and Gingerich 

(1998) have shown, however, that in areas where

46 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
20°50' 156°07' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Alters equal area 

projection, standard parallels 20°39'30" and 20C57'30", 

central meridian 156°20'15"

2,000

I

4,000 FEET

__I

I 

500 1,000 METERS

EXPLANATION

——700——

99.

LINE OF EQUAL ALTITUDE OF TOP OF 

CONVERGENCE ZONE-Interval 200 feet. 

Datum is mean sea level. Dashed where 

approximate

TEST HOLE AND NUMBER

(1,201) TOP OF CONVERGENCE ZONE, IN FEET 

ABOVE MEAN SEA LEVEL

Figure 25. Estimated altitude of the top of the convergence zone, Nahiku area, Maui, Hawaii.

Vertical Thickness of the Fresh Ground-Water Lens 47
20°50' 156°07'

20°49'

20°48'

156°06'

I

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area 

projection, standard parallels 20°391 30" and 20°57'30", 

central meridian 156°20'15"

2,000

I

r

500

4,000 FEET

__I

1,000 METERS

EXPLANATION

— 400— LINE OF EQUAL ALTITUDE OF BOTTOM OF 

CONVERGENCE ZONE-Interval 100 feet. 

Datum is mean sea level

99 TEST HOLE AND NUMBER

(548) BOTTOM OF CONVERGENCE ZONE, IN FEET 

ABOVE MEAN SEA LEVEL

Figure 26. Estimated altitude of the bottom of the convergence zone, Nahiku area, Maui, Hawaii.

48 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
SOUTH EXPLANATION NORTH PACIFIC OCEAN

CONVERGENCE ZONE ZONE OF HIGH PERMEABILITY 

HANA VOLCANICS 

KULAVOLCANICS 

HONOMANU BASALTWATER MOVEMENT BASED ON 

CURRENT-METER DATA

LINE OF SECTION AND 

TEST HOLE LOCATIONS

Altitude of Big Spring

VERTICAL EXAGGERATION x4Figure 27. Convergence zone, zone of high permeability, and well logs in selected test holes in the Nahiku area, Maui, Hawaii.
Table 8. Calculated altitude (in feet below sea level) of the midpoint of the transition zone between freshwater and 

saltwater, Nahiku area, Maui, Hawaii

Vertical hydraulic 

gradient 

Test hole (feet/feet)

85 0.66

87 0.60

88 0.10

89 0.51

90 0.42

Bottom hole 

altitude 

(feet)

12

below sea level

below sea level

below sea level

17

Altitude of the midpoint of the 

/TO transition zone 

(feet) (feet)

344

317

53

223

446

-502

-507

-424

-417

-1,002

significant vertical movement of ground water exists 

(such as in the Nahiku area) the depth to the freshwatersaltwater interface can best be approximated from the 

relation:

= -h0 / (0.025 (1)

for:

z = altitude relative to sea level of the midpoint in 

the transition zone between freshwater and 

saltwater,

h0 = head in the well at sea level, and 

A/z/Az = vertical hydraulic gradient measured over the

total open interval of the well. 

Equation 1 was used to estimate the altitude relative to sea level of the freshwater-saltwater interface 

at the deepest test holes in the study area and the results 

(table 8 and fig. 28) are consistent areally. Calculated 

depth to the interface ranges from 417 ft below sea 

level at test hole 89 to 1,002 ft below sea level at test 

hole 90.

HYDRAULIC CHARACTERISTICS OF THE 

ROCK UNITS

The only information available for the horizontal 

hydraulic conductivity of the rocks in the Nahiku area 

is from an aquifer test on Kuhiwa well done by Maui 

Pineapple, Inc., and the USGS in May 1992. This well 

is open to the aquifer between the altitudes of 131 to 

471 ft above sea level. Results of a 7-day aquifer test, 

from May 12 through May 19, 1992, indicate an average value for the hydraulic conductivity of the rock 

between the altitudes tapped by the well of 0.8 ft/d 

(unpub. aquifer-test archives, U.S. Geological Survey, 

Honolulu). The horizontal hydraulic conductivity of

individual clinker zones in the interval is probably 

higher.

An estimate of an upper bound for the effective 

or equivalent vertical hydraulic conductivity of the 

rock units, KE (Domenico and Schwartz, 1990, p. 69), 

can be calculated from water-budget information and 

the average vertical hydraulic gradients shown in table 

5. The average hydraulic gradient over a horizon consisting of many rock units with varying thickness and 

vertical hydraulic conductivity values would be a function of the rate of water moving vertically through the 

horizon and the vertical hydraulic conductivity, Kv, and 

thickness, m, of each rock unit according to the form of 

Darcy's Law:

(2)

where:

vz is the vertical rate of ground-water 

movement per unit area,

is average vertical hydraulic gradient, 

lve and

KE is

For mi equal to the thickness of an individual 

layer within the horizon and Kv equal to the vertical 

hydraulic conductivity of that layer. The summation 

would be for all layers in the horizon.

Test holes 65,74, 82, 83, 86, and 93 are all in the 

Hanawi drainage basin (fig. 2) and above the lower 

gage (5090) (fig. 11). The average hydraulic gradient 

for both upward and downward movement calculated 

for those test holes from table 5 is 0.56. Mean annual 

recharge above the gage is 37.9 Mgal/d over an area of 

13.94 x 107 ft2 (Shade, 1999). This converts to an average rate of water movement per unit area of 3.7 x 10"2

50 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
20°50' 156°07' 156°06'

20°49' -

20°48' -

Base modified from U.S. Geological Survey 

digital data, 1:24,000,1983, Albers equal area 

projection, standard parallels 20C39'30" and 20°57'30", 

central meridian 156°20'15"

4,000 FEET

__I

500 1,000 METERS

EXPLANATION

• -500- - LINE OF EQUAL ALTITUDE OF FRESHWATERSALTWATER INTERFACE-Interval, in feet, 

is variable. Datum is mean sea level. Dashed 

where approximate

87. TEST HOLE AND NUMBER

(-507) ALTITUDE OF FRESHWATER-SALTWATER INTERFACE, 

IN FEET BELOW MEAN SEA LEVEL

Figure 28. Calculated altitude of the freshwater-saltwater interface, Nahiku area, Maui, Hawaii.

Hydraulic Characteristics of the Rock Units 51
ft/d above the lower gage. The average hydraulic gradient of 0.56 and the average rate of water movement 

(3.7 x 10~2 ft/d) can be used in equation 2 to solve for 

KE. This value of Kg, 0.07, should be considered to be 

an upper bound on the value of KE in the area, because 

at any given location in the flow system, water generally would be moving both horizontally and vertically 

whereas this calculation assumes only vertical movement of water.

SUMMARY AND CONCLUSIONS

The Nahiku area is underlain by lavas of the 

Honomanu Basalt, the Kula Volcanics, and the Hana 

Volcanics. The Hana Volcanics forms the surface of 

most of the area. Stearns and Macdonald (1942) 

assumed that the ground-water system in the Nahiku 

area consists of a succession of perched water bodies in 

the Kula Volcanics, a perched artesian water body (of 

limited areal extent) in the upper part of the Honomanu 

Basalt and a basal water body with water levels 5 to 10 

feet above sea level in the Honomanu Basalt. The Hana 

Volcanics, which overlies the Kula Volcanics, was 

assumed to be dry as was the Honomanu Basalt outside 

of the perched artesian aquifer and the basal aquifer. 

Streams were considered perennial in areas where they 

intersected perched water bodies in the Kula Volcanics, 

but otherwise lost water or were intermittent. Springs, 

which are widespread in the area, were believed to 

issue from perched water bodies in the Kula Volcanics 

except at the shoreline where they also issued from the 

basal aquifer.

The underlying premise of Stearns and Macdonald (1942) for the relationship among geology, 

streamflow, and ground-water occurrence was that the 

lava flows of all three rock units were considered 

highly permeable and unable to perch water. Despite 

this assumption, Stearns and Macdonald (1942) indicate that the Kula Volcanics, when viewed as a unit, 

"contains enough more or less impermeable layers, 

even though discontinuous, to retard greatly the downward percolation of water in areas where 100 to 400 

inches of rain falls annually." Stearns and Macdonald 

state that because high-level water occurred only as 

perched water in the Kula Volcanics, streamflow was 

perennial only where streams intersected high-level 

water. However, they indicate that the source of water 

to Big Spring was a "perched" artesian water body in 

the Honomanu Basalt.

In general, the modes of occurrence of ground 

water in Hawaii have historically been divided into 

high-level and basal water bodies. Inherent in this 

description is the assumption that the permeability of 

the volcanic rocks that constitute the major bulk of the 

islands is uniformly high (averaging 2,000 feet per 

day). As a consequence, high-level water bodies are 

believed to result only from the impedance of the lateral movement of ground water by dikes in rift zones or 

from the impedance of the vertical movement of 

ground water by low-permeability features. Water levels in high-level ground-water bodies reach altitudes of 

several thousand feet above sea level. Basal water bodies with water levels of 30 feet or less form in the flank 

flows that extend beyond rift zones.

The relatively high value of hydraulic conductivity assumed for the volcanic rocks that form basal aquifers in Hawaii probably results from the young age of 

the flows and from their limited thickness (less than 10 

feet on the average). In many areas of the State, such as 

east Maui and Kauai, however, the underlying lava 

flows are relatively thick. In these areas the hydraulic 

conductivity of the volcanic rocks is much lower (three 

orders of magnitude) than that normally associated 

with that of basal aquifers.

The assumption by Stearns and Macdonald 

(1942) that the lavas of the three rock units underlying 

the Nahiku area are highly permeable was not founded 

on field data from this area. In contrast to this assumption, an aquifer test conducted at Kuhiwa well in 1992 

yielded a value for the horizontal hydraulic conductivity of the upper 340 feet of the Honomanu Basalt equal 

to 0.8 feet per day, or about three orders of magnitude 

lower than values normally assumed for the volcanic 

rocks in the State.

The alternative concept to that of Stearns and 

Macdonald (1942) for the occurrence of ground water 

in the Nahiku area, supported by this report, is that 

ground water occurs as a vertically extensive water 

body extending from below sea level into the Hana 

Volcanics. This concept is based on the assumption that 

the value for the horizontal hydraulic conductivity of 

the upper part of the Honomanu Basalt identified by the 

aquifer test at Kuhiwa well is more representative of 

the hydraulic properties of the rocks in the area than is 

the assumption by Stearns and Macdonald (1942) that 

the rocks are highly permeable, and a reinterpretation 

of existing data.

Considerable evidence beyond the results of the 

aquifer test at Kuhiwa well supports the alternative

52 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
concept for ground-water occurrence. Much of this evidence contrasts sharply with some of the basic conclusions reached by Stearns and Macdonald (1942). Some 

100 test holes were constructed during a test-drilling 

program during the 1930's and 1940's with geologic 

and hydrologic data reported for 88 of these holes. In 

general, Stearns and Macdonald's (1942) concept of 

ground-water occurrence would have been substantiated had holes in each of the three geologic units in the 

area been dry. However, water was reported in all 88 of 

the 100 test holes for which hydrologic data were 

recorded.

Although Stearns and Macdonald (1942) 

assumed that the rocks of the Hana Volcanics are unsaturated, the results of the test-drilling program indicate 

that an extensive body of freshwater exists in these 

rocks throughout the Nahiku area. In addition, despite 

the assumption by Stearns and Macdonald (1942) that 

streams overlying the Hana Volcanics are not perennial, streamflow is perennial in streams underlain by 

the Hana Volcanics owing to the ground-water discharge.

Not only was water found in the Hana Volcanics 

throughout the area, but the water level in many of the 

test holes remained above the top of the Kula Volcanics 

as the holes were deepened from the Hana and Kula 

Volcanics into the Honomanu Basalt in areas outside of 

the artesian water body. This result would not be possible if the occurrence of ground water in the area were 

consistent with the concept of Stearns and Macdonald 

(1942). Such a result requires that either (1) numerous 

perched water bodies exist throughout the stratigraphic 

column from the Hana Volcanics to the bottom of the 

test holes in the Honomanu Basalt, and cascading water 

into the holes maintains a water level above the top of 

the Kula; or (2) the rocks are saturated from the Hana 

Volcanics on down. Either of these conclusions would 

present a different conceptual framework of groundwater occurrence in the area than that of Stearns and 

Macdonald (1942), but given the lack of interstratified 

perching beds in the Hana Volcanics and the Honomanu Basalt, the first interpretation is the least likely.

Water remained in the test holes once encountered and the amount of water in the holes generally 

increased as each hole was deepened. These results are 

consistent with the concept that the area is underlain by 

a vertically extensive water body. The Stearns and 

Macdonald (1942) mode of ground-water occurrence 

would require the test holes to be dry in the Hana Volcanics and contain water when perched water bodies

were encountered in the Kula Volcanics. Below these 

bodies the amount of water in the borehole would be 

expected to decrease. Ultimately as the hole was deepened to greater depths into unsaturated but presumably 

permeable rock, the Stearns and Macdonald mode of 

ground-water occurrence requires a dry hole or cascading water from perched water bodies above the bottom 

of the hole could cause the presence of a limited, but 

decreasing amount of water in the borehole.

Five test holes and Kuhiwa well were drilled to 

depths near to or below sea level and water levels in 

these holes failed to identify the existence of a basal 

water body with water levels 5 to 10 feet above sea 

level. Water levels ranged from 47 feet at a distance of 

about 300 feet from the ocean to 1,126 feet at Kuhiwa 

well located about 2 miles inland of the ocean, which 

further supports the existence of a vertically extensive 

ground-water system.

The results of a numerical model of the Hanawi 

Stream basin indicate that a vertically extensive 

ground-water body is possible with water levels consistent with those obtained from the test-drilling program 

(Gingerich, 1998). The numerical model used values of 

the hydraulic properties of the rocks obtained for the 

Honomanu Basalt from the Kuhiwa well aquifer test 

and the effective vertical hydraulic conductivity of the 

rocks discussed in this report. Precipitation in the area 

ranges from 160 to 350 inches per year and about 60 

percent of this becomes ground-water recharge (Shade, 

1999). The simulated vertically extensive groundwater body results directly from the combination of 

high ground-water recharge rates, the low hydraulic 

conductivity of the rocks, and the geometry of the 

ground-water flow system.

The general movement of ground water in the 

area, assuming a vertically extensive water body, is laterally toward the ocean and streams and vertically 

downward. The vertical movement of the water is generally downward outside of the artesian water body 

except in the artesian water body and near the ocean 

where movement is upward. The water body extends 

from below sea level up into the Hana Volcanics. The 

water table is in the Hana Volcanics and ranges in altitude from about 47 feet near the shoreline to about 

1,400 feet 2 miles inland. The artesian water body is in 

the upper part of the Honomanu Basalt and has limited 

areal extent.

The area of greatest ground-water discharge into 

Hanawi Stream, including Big Spring, corresponds to a 

zone of high permeability located an average 220 feet

Summary and Conclusions 53
above the artesian water body into which water is moving from above and below. The vertical zone in which 

water is converging toward the high permeability zone 

is large, 420 feet on average. The bottom of this zone is 

the artesian water body while the top is demarked by a 

horizon wherein water levels abruptly declined as test 

holes were deepened.

Despite the relatively high water table in the 

area, the depth to the freshwater-saltwater interface is 

probably much less than that which would be predicted 

from the Ghyben-Herzberg equation. This results from 

the loss of head in the vertical direction which averages 

about 0.47 feet per feet.

In conclusion, the preponderance of hydrologic 

data supports the existence of a vertically extensive 

aquifer in the Nahiku area, east Maui, and that the 

source of Big Spring is a large zone of high permeability adjacent to the spring. This research and the work of 

Izuka and Gingerich (1998) on the island of Kauai may 

indicate that vertically extensive aquifers are much 

more prevalent than previously thought; therefore, this 

concept could be further explored as a controlling 

mechanism for ground-water movement and occurrence on other volcanic islands.

REFERENCES CITED

Cooper, H.H., Jr., Bredehoeft, J.D., and Papadopulos, I.S., 

1967, Response of a finite-diameter well to an instantaneous charge of water: Water Resources Research, v. 3, 

no. 1, p. 263-269.

Domenico, P.A., and Schwartz, F.W., 1990, Physical and 

chemical hydrogeology: New York, Wiley, 824 p.

Giambelluca, T.W., 1986, Land-use effects on the water balance of a tropical island: National Geological Society, 

National Geographic Research, v. 2, p. 125-151.

Gingerich, S.B., 1998, Numerical modelling of vertically 

extensive groundwater bodies in Maui, Hawaii: an 

alternative to perched aquifers, in Johnson, A.I. and 

Fernandez-Jaurequi, C.A., eds., Hydrology in the 

Humid Tropic Environment [Proceedings of a symposium held November 1996, Kingston, Jamaica], International Association of Hydrological Sciences 

Publication no. 253, 167-174.

Institute of Hydrology, 1980a, Low flow studies: Wallingford, Oxon, United Kingdom, Report no. 1, 21 p.

Institute of Hydrology, 1980b, Low flow studies: Wallingford, Oxon, United Kingdom, Report no. 3, p. 12-19.

Izuka, S.K., and Gingerich, S.B., 1998, Ground water in the 

southern Lihue basin, Kauai, Hawaii: U.S. Geological 

Survey Water-Resources Investigations Report 98- 

4031, 71 p.

Izuka, S.K., and Gingerich, S.B., 1998, Estimation of the 

depth to the fresh-water/salt-water interface from the 

vertical head gradient in wells in coastal and island 

aquifers: Hydrogeology Journal, v. 6, no. 3, p. 365-373.

Langenheim, V.A.M., and Clague, D.A., 1987, The

Hawaiian-Emperor volcanic chain, part II, stratigraphic 

framework of volcanic rocks of the Hawaiian Islands, 

chap. 1 of Decker, R.W, Wright, T.L., and Stauffer, 

PH., eds., Volcanism in Hawaii: U.S. Geological Survey Professional Paper 1350, v. 1, p. 55-84.

Mink, J.F., and Lau, L.S., 1980, Hawaiian groundwater geology and hydrology, and early mathematical models: 

University of Hawaii Water Resources Research Center 

Technical Memorandum Report 62, 74 p.

Peterson, F.L., 1981, Geological and hydrological framework: A history of development in Groundwater in 

Hawai'i: A century of progress, proceedings of the artesian water centennial symposium, Fujimura, F.N., and 

Chang, W.B.C., eds., University of Hawaii Water 

Resources Research Center, 260 p.

Shade, P.J., 1999, Water budget of east Maui, Hawaii: U.S. 

Geological Survey Water-Resources Investigations 

Report 98-4159, 35 p.

Stearns, H.T., and Macdonald, G.A., 1942, Geology and 

ground-water resources of the island of Maui, Hawaii: 

Hawaii Division of Hydrography Bulletin 7, 344 p., 

2 pis. in pocket.

Takasaki, K.J., and Yamanaga, George, 1970, Preliminary 

report on the water resources of northeast Maui: State 

of Hawaii Department of Land and Natural Resources 

Circular C60, 41 p.

U.S. Geological Survey, [1924 to 1998] Water resources data 

for Hawaii and other Pacific areas, water years 1923 to 

1997: Water-Data Reports, Honolulu, Hawaii, variously paged.

U.S. Geological Survey, 1976, Water resources data for 

Hawaii and other Pacific areas, water year 1975: WaterData Report HI-75-1, Honolulu, Hawaii, p. 250.

Wahl, K.L., and Wahl, T.L., 1988, Effects of regional

ground-water level declines on streamflow in the Oklahoma panhandle in Proceedings of the American Water 

Resources Association Symposium on Water-Use Data 

for Water Resources Management, August 1988.

54 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
APPENDIX A: METHOD OF WATER-LEVEL 

DATA COLLECTION AND WATER LEVELS 

IN SELECTED TEST HOLES

Method of Water-Level Data Collection

The water-level data and descriptions of methods for collecting the data comes from unpublished 

well logs on file at the USGS, Honolulu. As discussed 

in the section "Water levels in the Hana Volcanics," 

water-level data were collected in 88 of the 100 test 

holes and although the procedure for collecting waterlevel data was not consistent, water levels were measured each day in the deeper test holes as drilling progressed. Water levels generally were measured in the 

test holes before the start of the day's drilling although 

some measurements also were made at the end of the 

day. For the most part, water-level measurements were 

made through the center of the drill rod after the drill 

string was lowered to the bottom of the hole. The core 

bit usually was at the bottom of the hole or within a foot 

or so of the bottom when the water level was measured.

Water levels measured inside the drill rod with 

the drill rod lowered to a given depth in a borehole 

probably provide a closer approximation of the composite head in the borehole below the drill bit than of 

the water level in the entire borehole. This is because 

the annular space between the drill rod and the borehole was only 3/32 in. (the diameter of the borehole was 

l-l/2 in. and the outside diameter of the drill rod was 

l-5/i6 in.). Given this small annular space between the 

borehole and the drill rod, and the length of borehole 

the drill rod occupied when the measurements were 

made, it is reasonable to expect a measurable resistance 

to vertical flow and some head loss as a result.

In a ground-water flow system wherein heads 

decline with depth, as in the Nahiku area outside the 

artesian water body, the water level in an open borehole 

completed to a given depth will be some composite of 

the heads encountered to that depth. As drilling 

progresses, water levels will decline in the borehole 

because the composite head will decline. Because 

heads are declining with depth, and because the water 

level in the borehole is some composite of the range in 

head over the length of the borehole, the water level in 

the borehole would be expected to always be below the 

actual water table. The head at the bottom of the hole 

would be the lowest head in the hole. Because the water 

level in the boreholes was measured inside the drill rod 

with the drill bit at or near the bottom of the hole, it is 

reasonable to assume that the resulting value of water

level more closely approximates the head at the bottom 

of the hole than the composite water level that would 

exist in an open borehole of the same depth.

Water-level measurements made in five test 

holes (65, 85, 87, 90, 92) completed in the Honomanu 

Basalt support the concept that the water level measured inside the drill rod with the bit at the bottom of 

the hole was the lowest head in the hole. These measurements showed that water levels in the boreholes 

were actually higher than that indicated by the measurement inside the drill rod with the bit at the bottom 

of the hole. Following the measurement of the water 

level in these holes with the drill bit at the bottom of the 

hole, water levels also were measured in one of the following two ways: (1) For selected hole depths (generally the final hole depth), the water level was recorded 

inside the drill bit with the bit at the bottom of the hole 

after which the bit was raised from the bottom of the 

hole and the water level inside the drill rod was measured at successively higher altitudes in the borehole; 

or (2) water-level measurement was made as in (1) but 

a 1-in. pipe was initially inserted to the bottom of the 

hole. These two methods of measurement indicated 

that water levels were significantly higher in the boreholes than those measured inside the drill rod with the 

bit at the bottom of the hole. The highest water levels 

were associated with the highest altitudes of either the 

drill bit or the pipe. The difference between the water 

level measured with the drill bit at the bottom of the 

hole and that measured using the above techniques 

ranged from 171 to 493 ft and averaged 325 ft (table 

Al).

The annular space between the borehole and the 

1-in. pipe (0.25 in.) was greater than that between the 

drill rod and the borehole (3/32 in.) so that less resistance to vertical flow would be expected for a pipe 

measurement as compared with the measurement 

obtained inside the drill rod. Of interest is that both 

techniques indicated that head measured at any point in 

the borehole was higher than that measured at the bottom of the hole. Neither measurement technique would 

have been expected to indicate the actual or composite 

water level in the entire open borehole. Presumably, it 

was higher than that indicated by either of these techniques. A detailed discussion of the water-level measurements made in test holes 65, 85, 87, 90, and 92 is 

provided in the next section (Water Levels in Selected 

Test Holes").

Data obtained from the use of a current meter 

lowered in selected holes completed in the Honomanu

Appendix A: Method of Water-Level Data Collection and Water Levels in Selected Test Holes 55
Table A1. Water levels measured inside the drill rod with the bit at the bottom of the hole and using alternative methods at selec

AReeva

luation oftheOccu

•t

§

o

9

a

o 

3

c

3

Q.

1SJ.

5

5'

f*

(D

OJ 3" 

5?

compieiea in ine nonomanu Dasaii, NaniKU area, iviaui, nawaii

[Values in feet; datum is mean sea level; 1 and 2 indicate method of water-level measurement; 1, 

Geological Survey, Honolulu]

Test 

hole

83

92

94

99

100

65

86

Location

artesian

artesian

artesian

artesian

artesian

above artesian

above artesian

Land 

surface 

altitude

945

902

796

1,578

1,845

1,066

1,494

Hole 

depth

790

754

596

1,024

1,072

529

817

Bottom 

of hole 

altitude

155

148

200

554

773

537

677

Depth in 

Honomani 

Basal

343

312

191

337

12

77

233

Depth 

i to water

1

709

561

130

451

669

362

614

2

230

86

98

385

400

184

180

bit at bottom; 2, alternative method; datum is mean sea level

Altitude of 

water level

1

236

341

666

1,127

1,176

704

880

2

715

816

698

1,193

1,445

882

1,314

Water level 

relative to top 

of Kula 

Volcanics

1

-536

-350

52

-260

-307

-144

-371

2

-57

125

84

-194

-38

34

63

Water level 

above bottom 

of hole 

1

81

193

466

573

403

167

203

2 

560

668

498

639

672

345

637

12 outside artesian 1,282 806 476 170 508 200 774 1,082 -344 -36 298 606 

87 outside artesian 465 738 -273 312 415 105 50 360 -157 153 323 633 

near to or 

below sea 

level

90 outside artesian 864 847 17 243 411 240 453 624 30 201 436 607 

near to or 

below sea 

level

97 outside artesian 826 595 231 232 345 298 481 528 -45 2 250 297 

85 near to or below 1,003 

sea level

991 12 448 666 173 337 830 -440 53 325 818 
Basalt also indicated that water levels in the borehole 

were higher than the value obtained from the waterlevel measurement inside the drill rod with the bit at the 

bottom of the hole. A directional current meter was 

lowered into the water column in some of the boreholes 

and used to determine the direction of water movement 

at selected altitudes within the column. Although the 

water level was not directly measured during this procedure, the presence of moving water at a given altitude was detected. It was possible to compare the water 

level measured inside the drill rod with the bit at the 

bottom of the hole to the highest altitude of water in the 

borehole where water movement was recorded in seven 

of the test holes (12, 83, 86, 94, 97, 99, and 100). The 

latter altitudes were always greater than the former. 

Differences ranged from 32 to 479 ft and averaged 234 

ft (table Al). A detailed discussion of the data obtained 

from the use of the directional current meter is also 

contained in the next section ("Water Levels in 

Selected Test Holes").

Water Levels in Selected Test Holes

Water-level data collected at test hole 90 demonstrates that the altitude of the water level inside the drill 

rod increased as the drill rod was raised 547 ft from the 

bottom of this hole (table A2). The altitude of the water 

level in test hole 90 generally declined as the hole was 

being drilled. The altitude of the water level with the 

drill rod at the bottom of the hole was 453 ft. Following 

completion of the hole, the drill rod was raised from the 

bottom and the depth to water recorded at selected altitudes in the hole as the drill rod was raised. The altitude 

of the water level measured inside the drill rod 

increased from 453 to 624 ft as the drill rod was raised 

544 ft. The total increase in the altitude of the water 

level in the borehole was 171 ft.

A somewhat similar set of data is available from 

test hole 65. As with test hole 90, the altitude of the 

water level in the test hole generally decreased as the 

test hole was deepened. A 3/4-inch pipe was inserted 

into the hole after the hole was completed, and water 

levels were measured as the pipe was progressively 

raised to higher altitudes in the hole (table A3). The 

altitude of the water level measured inside the pipe 

increased from 704 to 882 ft as the pipe was raised 336.

The relation between the altitude of the water 

level and the depth of the pipe or drill rod is just the 

opposite of that which would be expected if the displacement of water by the drill rod (or pipe) played a 

major role in the depth of water inside the drill rod. The 

observed relation is consistent, however, with what 

would be expected if the rocks are saturated below the 

first water encountered during drilling and the general 

movement of water is downward.

These results indicate that, for those test holes in 

which water levels generally declined as the test holes 

were deepened, the actual water level in the test hole 

may have been higher, and perhaps much higher, than 

that obtained with the drill bit on the bottom of the hole. 

Other test holes for which there is data that pertain to 

this discussion are test holes 85, 87, 92, 12, 83, 86, 94, 

97, 99, and 100.

The altitude of the water level measured inside 

the drill rod with the bit at the bottom of the hole at test 

hole 87 was 50.3 ft at the final hole depth of 737.8 

(272.8 ft below sea level) (table A4). Another waterlevel measurement was made the following day with 

the drill bit at 562.8 ft above the bottom of the hole. The 

altitude of the water level was 360 ft, or 309.7 ft higher 

than the water level measured with the bit at the bottom 

of the hole.

The altitude of the water level measured inside 

the drill rod at test hole 92 ranged from 820 to 817 ft for 

bottom hole altitudes ranging from about 330 to 157 ft 

(table A5). At a final bottom hole altitude of 148 ft, the 

altitude of the water level decreased to 341 ft. The altitude of water level measured 2 days after completion of 

the test hole was 816 ft. This measurement was made 

with the drill bit at an altitude of 253 ft which is 105 ft 

above the bottom of the hole. The difference between 

the two water-level measurements (475 ft) could indicate a lower hydraulic head at the final hole depth or a 

transient filling of a "hole" reported by the driller 

between the altitudes of 151 and 148 ft.

The altitude of the water-level measurement at 

test hole 85 was 337 ft at the final bottom hole altitude 

of 12 ft. This water-level measurement was made 

inside a 1-in. pipe lowered to the bottom of the hole 

(table A6). Following this measurement, the pipe was 

removed from the hole and reinserted. The hole was 

bridged at an altitude of 205 ft, however, precluding the 

possibility of lowering the pipe to the bottom. Iron filings, salt, and humus were used to fill the hole between 

the altitudes of 12 to 212 ft after which the pipe was 

lowered to an altitude of 212 ft. The altitude of the 

water level measured inside the pipe at this depth was 

830 ft.

Appendix A: Method of Water-Level Data Collection and Water Levels in Selected Test Holes 57
Table A2. Selected water-level measurements at test hole 90, Nahiku area, Maui, Hawaii

[--, not measured. Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Date

Aug. 20, 1942

Aug. 21, 1942

Aug. 22, 1942

Aug. 29, 1942

Sept. 3, 1942

Sept. 4, 1942

Sept. 5, 1942

Sept. 7, 1942

Sept. 8, 1942

Sept. 9, 1942

Sept. 10, 1942

Sept. 12, 1942

Sept. 14, 1942

Sept. 15, 1942

Sept. 16, 1942

Oct. 26, 1942

Oct. 27, 1942

Dec. 7, 1942

Dec. 9, 1942

Dec. 9, 1942

Dec. 9, 1942

Dec. 9, 1942

Dec. 9, 1942

Dec. 9, 1942

Hole depth 

(feet)

180.5

191.4

211.5

261.8

281.9

281.9

299.3

307.8

312.1

322.7

338.5

359.2

371.1

385.4

402.8

516.3

529.7

830.3

847.3

847.3

847.3

847.3

847.3

847.3

Bottom hole 

altitude 

(feet)

683.5

672.6

652.5

602.2

582.1

582.1

564.7

556.2

551.9

541.3

525.5

504.8

492.9

478.6

461.2

347.7

334.3

33.7

16.7

16.7

16.7

16.7

16.7

16.7

Method of Depth to drill bit 

measurement (feet)

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

chop bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

179

190

211.5

259

279

279

299

304.5

312.1

319

338.5

359.2

369

385.4

399

514

529

829

844

700

600

500

400

300

Depth to water 

(feet)

130.6

131

--

212.6

231.5

231.5

231.5

231.5

231.5

231.5

230.1

227.1

223.4

226.4

231.8

402.8

407.1

412.5

411

413.4

413.4

412

262.4

240

Water-level 

altitude 

(feet)

733.4

733.0

--

651.4

632.5

632.5

632.5

632.5

632.5

632.5

633.9

636.9

640.6

637.6

632.2

461.2

456.9

451.5

453.0

450.6

450.6

452.0

601.6

624.0

Table A3. Selected water-level measurements at test hole 65, Nahiku area, Maui, Hawaii

[--, not known. Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Date

Aug. 19 (1937?)

Sept. 6 (1937?)

Sept. 20 (1937?)

Sept. 29 (1937?)

Nov. 11 (1937?)

Nov. 12 (1937?)

--

--

-

--

-

--

Hole depth 

(feet)

18

140

152

171

395

409

529

529

529

529

529

529

Bottom hole 

altitude 

(feet)

1,048

926

914

895

671

657

537

537

537

537

537

537

Method of Depth to bottom Depth to water 

measurement of pipe (feet) (feet)

--

-

--

--

--

—

3/4-inch pipe

3/4-inch pipe

3/4-inch pipe

3/4-inch pipe

3/4-inch pipe

3/4-inch pipe

--

-

--

--

-

-

526

426

306

232

190

148

15

93

90

99

121

121

362

349

280

221

184

no water

Water-level 

altitude 

(feet)

1,051

973

976

967

945

945

704

717

786

845

882

--

58 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Table A4. Selected water-level measurements at test hole 87, Nahiku area, Maul, Hawaii

[--, no data. Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Date

Mar. 6, 1942

Mar. 6, 1942

Mar. 19, 1942

Mar. 19, 1942

Mar. 21, 1942

Mar. 23, 1942

Mar. 25, 1942

Mar. 26, 1942

Mar. 27, 1942

Mar. 28, 1942

Mar. 28, 1942

Mar. 30, 1942

Mar. 31, 1942

Mar. 31, 1942

Mar. 31, 1942

Mar. 31, 1942

Apr. 1, 1942

Apr. 2, 1942

Apr. 2, 1942

Apr. 3, 1942

Apr. 3, 1942

Apr. 4, 1942

Apr. 6, 1942

Apr. 6, 1942

Apr. 7, 1942

Apr. 7, 1942

Apr. 7, 1942

Apr. 8, 1942

Apr. 8, 1942

Apr. 9, 1942

Apr. 10, 1942

Apr. 11, 1942

Apr. 11, 1942

Apr. 14, 1942

Apr. 16, 1942

Apr. 17, 1942

Apr. 17, 1942

Apr. 18, 1942

Apr. 18, 1942

Hole depth 

(feet)

84.4

194.2

356.3

375.9

415.4

445

502

502

521.7

529.7

540.3

545.1

558

574.6

574.6

574.6

579.6

588.6

600.1

603.4

608.6

615.3

623.3

639

639

645.2

655.1

655.1

666.3

692

690

707

724

724

732

732

737.8

737.8

737.8

Bottom hole 

altitude 

(feet)

380.6

270.8

108.7

89.1

49.6

20

-37

-37

-56.7

-64.7

-75.3

-80.1

-93

-109.6

-109.6

-109.6

-114.6

-123.6

-135.1

-138.4

-143.6

-150.3

-158.3

-174

-174

-180.2

-190.1

-190.1

-201.3

-227

-225

-242

-259

-259

-267

-267

-272.8

-272.8

-272.8

Method of Depth of drill bit 

measurement (feet)

blow

chop bit

diamond bit

blow

blow

blow

blow

chop bit

diamond bit

diamond bit

diamond bit

chop bit

diamond bit

chop bit

chop bit

chop bit

chop bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

chop bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

chop bit

chop bit

diamond bit

blow

chop bit

-

194.2

356.3

-

-

-

-

502

521.7

529.2

540.3

545.1

558

574.6

528

348

579.6

588.6

600.1

603.4

348

615

623

638.7

638.7

645

655

655

665

690

690

705

723.7

724

-

732

737

-

175

Depth to water 

(feet)

78.6

89.5

82.9

77.6

78.6

71

76

102

101.9

102.7

102.5

104

104.3

104.1

103.6

100.1

102.2

106.3

105

97.1

94.6

135.9

127.5

107.5

107.5

113.4

123.5

122.5

123.9

193.3

193.3

188.7

191.2

188.6

183.6

415

414.7

84

105

Water-level 

altitude 

(feet)

386.4

375.5

382.1

387.4

386.4

394.0

389.0

363.0

363.1

362.3

362.5

361.0

360.7

360.9

361.4

364.9

362.8

358.7

360.0

367.9

370.4

329.1

337.5

357.5

357.5

351.6

341.5

342.5

341.1

271.7

271.7

276.3

273.8

276.4

281.4

50.0

50.3

381.0

360.0

Appendix A: Method of Water-Level Data Collection and Water Levels in Selected Test Holes 59
Table A5. Selected water-level measurements at test hole 92, Nahiku area, Maui, Hawaii 

[Datum is mean sea level; data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Date

Mar. 17, 1943

Mar. 18, 1943

Mar. 23, 1943

Mar. 24, 1943

Mar. 31, 1943

Apr. 9, 1943

Apr. 10, 1943

Apr. 16, 1943

Apr. 17, 1943

Apr. 19, 1943

Hole depth 

(feet)

467

481

502

519

572

681

707

745

754

754

Bottom hole 

altitude 

(feet)

435

421

400

383

330

221

195

157

148

148

Method of 

measurement

chop bit

chop bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

diamond bit

chop bit

Depth of drill bit 

(feet)

464

479

499

518

569

684

704

744

752

649

Depth to water 

(feet)

222

157

157

157

85

85

82

85

561

86

Water-level 

altitude 

(feet)

680

745

745

745

817

817

820

817

341

816

Table A6. Selected water-level measurements at test hole 85, Nahiku area, Maui, Hawaii

[Datum is mean sea level; --, no data. Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Date

Jan. 10, 1941

-

-

Apr. 3, 1941

Apr. 8, 1941

Apr. 12, 1941

-

-

Hole depth 

(feet)

517

804

804

865

900

951

991

991

Bottom hole 

altitude 

(feet)

486

199

199

138

103

52

12

12

Depth to drill bit 

Method of or pipe bottom 

measurement (feet)

drill bit

drill bit

1-inch pipe

diamond bit

diamond bit

diamond bit

1-inch pipe

1-inch pipe

517

—

804

865

900

951

991

*791

Depth to water 

(feet)

103

103/104

174

176

250

424

666

173

Water-level 

altitude 

(feet)

900

899

829

827

753

579

337

830

1 Iron filings were used to fill hole from 991 to 791 feet prior to water-level measurement. Driller notes that a little humus and salt were added from time to 

time as the filings were placed in hole

Table A7. Depth-to-water measurements made inside the drill rod and inferred from current-meter measurements at selected

test holes, Nahiku area, Maui, Hawaii

[Values in feet; datum is mean sea level; data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Test 

hole

12

83

86

94

97

99

100

Hole 

depth

806

790

817

596

595

1,024

1,072

Bottom hole 

altitude

476

155

677

200

231

554

773

Depth to water 

Inside drill bit

508

768

614

130

345

451

669

(A) 

Water-level

altitude 

Inside drill bit

774

177

880

666

481

1,127

1,176

Depth to water 

inferred from

current-meter 

measurement

200

230

180

98

298

385

400

(B) 

Water-level altitude 

inferred from

current-meter 

measurement

1,082

715

1,314

698

528

1,193

1,445

Difference 

between columns

(A) and (B) 

[(B)-(A)]

308

479

434

32

47

66

269

60 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
The data from test holes 12, 83, 86, 94, 97, 99, 

and 100 that pertain to this discussion are current-meter 

measurements that were made when these holes were 

completed, or, for selected hole depths, while drilling 

was in progress. To measure the direction of water 

movement, a directional current meter was placed at 

the bottom of the drill string and lowered into the hole. 

Current-meter measurements were then made at 

selected depths in each hole. Although as previously 

noted, the water level was not directly measured during 

this procedure, the presence of moving water was 

detected at specific altitudes. A comparison of the 

water level measured inside the drill rod with the bit at 

the bottom of the hole to the highest altitude of water in 

the borehole where water movement was recorded during the current-meter measurements indicated that the 

latter measurement was always greater than the former 

(table A7). The difference between the altitude of the 

water level measured at or near the bottom of test holes 

12, 83, 86,94,97,99, and 100 as indicated by measurements inside the drill rod and highest altitude of the 

water level in the borehole as indicated by currentmeter measurements was 308,538,434,32,47,66, and 

269 ft, respectively.

As shown in table A7, the altitude of the water 

level measured inside the drill rod at test hole 12 at a 

bottom hole altitude of 476 ft was 774 ft. Current-meter 

measurements made in the hole at this depth, however, 

indicated water moving downward between the altitudes of 1,082 to 492 ft thereby indicating the presence 

of water some 308 ft above that indicated by the measurement inside the drill rod.

The altitude of the water level measured inside 

the drill rod in test hole 83 (table A7) at the final bottom 

hole altitude of 155 ft was 236 ft. Current-meter measurements made in this hole 1 day after its completion 

indicated upward flow in the hole between the altitudes 

of 387 to 715 ft. This would indicate that the water 

level in the test hole was at least 479 ft higher than that 

indicated by the measurement inside the drill rod.

The altitude of the water level measured inside 

the drill rod at test hole 86 (table A7), at its final bottom 

hole altitude of 677 ft was 880 ft. Current-meter 

measurements made following completion of the hole, 

however, indicated that water was moving downward 

between the altitudes of 1,314 to 748 ft. Assuming a 

water level of at least 1,314 ft in the test hole, the difference between this value and that obtained from 

inside the drill rod at the bottom of the hole is 434 ft.

The altitude of the water level measured inside 

the drill rod at test hole 94 (table A7), at a bottom hole 

altitude of 200 ft was 666 ft. Current-meter measurements made at this hole depth indicated that water was 

moving downward between the altitudes of 698 to 618 

ft indicating that the water level in the hole was at least 

698 ft, or 32 ft higher than that indicated by the measurement inside the drill rod.

The altitude of the water level measured inside 

the drill rod at test hole 97 (table A7) was 481 ft at a 

bottom hole altitude of 231 ft. Current-meter measurements indicated that water began moving downward at 

an altitude of 528 ft, however, which would suggest 

that the altitude of the water level was at least 47 ft 

higher than that indicated by the drill rod measurement.

The altitude of the water level measured inside 

the drill rod in test hole 99 (table A7) at a bottom hole 

altitude of 554 ft was 1,127 ft. Current-meter measurements obtained at this depth, however, indicated water 

movement in the hole at 1,193 ft altitude, or 66 ft 

higher than the water level obtained inside the drill rod.

The altitude of the water level in test hole 100 

(table A7) measured inside the drill rod at a bottom 

hole altitude of 773 ft was 1,176 ft. Current-meter measurements, however, indicated that water began to 

move downward at an altitude of 1,445 ft.

The data shown in table A7 indicate that the 

actual water level in the hole was probably higher and 

potentially hundreds of feet higher than the measurement made inside the drill rod with the drill bit at the 

bottom of the hole.

All of the water levels in the test holes described 

above support the existence of the vertically extensive 

ground-water system.

APPENDIX B: GENERAL CONSIDERATIONS IN THE USE OF THE WATERLEVEL DATA

The main points in the previous discussion on 

the method for collecting water-level data are, for a 

ground-water flow system in which the movement of 

water is downward and heads decline with depth, (1) 

the water table and the composite head in the test hole 

(assuming an open hole) would be expected to be at 

higher altitudes than that indicated by the water level 

measured inside the drill rod with the bit at the bottom 

of the hole, and (2) the water level measured inside the 

drill rod with the bit at the bottom of the hole can only

Appendix B: General Considerations in the Use of the Water-Level Data 61
be assumed to approximate the head at the bottom of 

the hole. Despite these restrictions on the accuracy of 

the water-level data it can still be used as described 

below to examine the occurrence of ground water.

The first reported water levels in the test holes 

can be considered to closely approximate the water 

table in the area. Also, if water remained in the test 

holes as they were bored through the Hana Volcanics, 

clearly the presence of water in the Hana Volcanics is 

indicated.

In general, the remaining use of water levels 

measured inside the test holes with the bit at the bottom 

of the hole addresses the relations between water levels 

measured in the test holes and the geologic framework. 

In particular, it addresses the relation between the altitude of the water level measured inside the drill rod 

with the bit at the bottom of the hole at a given hole 

depth and the altitude of the top of the Kula Volcanics 

or the Honomanu Basalt. Absolute values are stated in 

this regard, but the significance of the discussion is not 

with regard to the absolute value.

The water level that would be used to assess this 

situation discussed immediately above would be the 

composite water level in the open borehole and not the 

hydraulic head at the bottom of the hole. The previous 

discussion on the accuracy of the water-level measurements indicated that the water level measured with the 

drill bit at the bottom of the hole represents a minimum 

value for the water level in the hole at a given depth. 

Thus, if the water level measured inside the test hole 

with the bit at the bottom of the hole indicates that the 

water level is above the top of the Kula Volcanics in a 

given test hole, then the composite water level in the 

hole should be above the top of the Kula also.

APPENDIX C: EFFECT OF DRILLING ON 

WATER-LEVEL MEASUREMENTS

Drilling imposes a stress on the ground-water 

system with the result that a difference may exist 

between water levels in the ground-water body before 

drilling and those measured during drilling. Factors 

that can influence this potential difference include, (1) 

the introduction of drilling fluid under pressure, (2) 

cascading water, (3) displacement of water by the drill 

string prior to measurement, and (4) movement of 

water in the open hole (both upward and downward at 

altitudes below the water level in the hole).

Introduction of Drilling Fluid Under 

Pressure

Ground water was encountered at shallow depths 

throughout the area and once present it remained in the 

test holes. The introduction of drilling fluid under pressure causes an upward movement of the drilling fluid 

and ground water in the annulus of the hole. As a result, 

ground water is effectively being pumped. Circulation 

of water and drilling fluid may continue to the surface, 

or may be lost in some permeable zone in the borehole, 

thereby introducing water into this area. It was not 

uncommon for the driller to report the presence of 

"leaks" as some holes were drilled in the EMI testdrilling program. This is particularly true for test holes 

in the area between Makapipi and Kuhiwa Streams. 

Such leaks were places where significant drilling pressure and thus fluid was lost. Water levels in the test 

holes often declined when these zones were encountered, although in some instances the decline was temporary. Even so, virtually all significant water-level 

declines in the test holes occurred under such circumstances.

Some indication of the possible effect that the 

introduction of drilling fluid under pressure may have 

had on water levels measured in the test hole can be 

discerned by comparing water levels measured at the 

end of the day's drilling to those measured before drilling the next morning. Wells, dates, and water levels for 

which this comparison can be made are shown in table 

Cl. For example, the water level in test hole 89 was 

measured on the afternoon of July 3, 1942 at 3:00 pm. 

Test hole depth was 320 ft. Depth to water in the hole 

was 120.5 ft. An identical water level was measured the 

next morning before drilling. Also shown in table Cl 

are water levels measured over a period of 2 or 3 days 

after drilling temporarily ceased. For example, the 

water level in test hole 90 was measured the morning 

of October 3, 1942 at a hole depth of 486.3 ft. The 

water level was 248.7 ft. The water level measured on 

October 5,1942 before additional drilling was the same 

as that measured on October 3.

If the introduction of drilling fluid under pressure 

caused a substantial change in the water level in a borehole from that prior to drilling, then water levels should 

have begun to measurably change after drilling 

stopped. This change could possibly continue for several months or more, but even so, water levels measured the next morning or several mornings after 

drilling ceased should indicate the presence of the

62 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Table C1. Depth to water in selected test holes for selected hole depths and times, Nahiku area, Maui, Hawaii

[Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Test hole

87

89

90

93

98

99

Date

Apr. 6, 1942

Apr. 7, 1942

Apr. 7, 1942

Apr. 8, 1942

Apr. 11, 1942

Apr. 14, 1942

July 3, 1942

July 4, 1942

July 15, 1942

July 16, 1942

July 20, 1942

July 21, 1942

July 21, 1942

July 22, 1942

July 22, 1942

July 23, 1942

Sept. 3, 1942

Sept. 4, 1942

Sept. 18, 1942

Sept. 19, 1942

Sept. 23, 1942

Sept. 24, 1942

Sept. 25, 1942

Sept. 26, 1942

Sept. 28, 1942

Sept. 29, 1942

Oct. 3, 1942

Oct. 5, 1942

Nov. 8, 1942

Nov. 9, 1942

Nov. 10, 1942

Dec. 2, 1942

Dec. 3, 1942

Dec. 3, 1942

Dec. 4, 1942

Dec. 5, 1942

Dec. 7, 1942

June 14, 1943

June 16, 1943

July 13, 1944

July 14, 1944

Aug. 9, 1944

Aug. 10, 1944

Sept. 21, 1944

Sept. 22, 1944

Sept. 23, 1944

Sept. 25, 1944

Nov. 4, 1944

Nov. 6, 1944

Feb. 24, 1945

Feb. 28, 1945

Mar. 7, 1945

Mar. 8, 1945

Time

2:00 pm

morning

2:30 pm

morning

2:00 pm

10:24 am

3:00 pm

morning

3:00 pm

morning

3: 12pm

morning

3:00 pm

morning

3:00 pm

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

morning

afternoon

morning

afternoon

morning

morning

morning

morning

morning

morning

morning

morning

morning

1:30 pm

morning

morning

morning

morning

morning

12:30 pm

11:00 am

3:30 pm

9:30 am

Hole depth 

(feet)

639

639

655.1

655.1

724

723

320

320

507.1

507.1

530.4

530.4

548.2

548.2

568.1

568.1

281.9

281.9

416.2

416.2

456.2

456.2

465.7

465.7

465.7

465.3

486.3

486.3

631.2

631.2

631.2

811.6

811.6

816.2

816.2

830.3

830.3

533.1

533.1

449.5

449.5

700

700

184.4

184.4

200

200

566.4

566.4

950.3

950.3

1,015.4

1,015.4

Depth to water 

(feet)

107.5

107.5

123.5

122.5

191.2

188.6

120.5

120.5

227.0

231.0

228.3

229.5

228.3

230.7

338.6

336.6

231.5

231.5

233.2

232.3

232.3

232.3

232.3

232.3

232.3

232.3

248.7

248.7

408.2

408.2

411.3

411

411

412.5

412.5

412.5

412.5

66.3

66.3

257.6

257.6

339.2

339.2

174.4

174.4

181.6

181.6

558.2

558.2

453.7

453

448

448

Appendix C: Effect of Drilling on Water-Level Measurements 63
change and provide some idea of its magnitude. The 

maximum difference between water levels at the end of 

a day's drilling and those measured 1 to 3 days later and 

before the resumption of drilling was 4 ft (at test hole 

89), although it was more common for the measurements to be identical or nearly so, indicating little effect 

on water levels.

Other data are available from test holes 74, 83, 

and 85 that indicate that the effects of drilling did not 

substantially alter water levels measured in the test 

holes from pre-drilling values. One-inch pipes perforated at the bottom, were placed in test holes 74, 83, 

and 85 following their completion and water levels 

were measured at selected times in the pipes as shown 

in table C2. These data indicate that little change in 

water levels occurred over a period of 1 to 2 months 

following completion of the holes. The maximum 

change was 6.6 ft at test hole 85. The maximum change 

after more than 2 years was 20.5 ft at test hole 74 and 

much of this change was probably seasonal. Given the 

altitude of the water levels recorded in the test holes, 

the data shown in tables Cl and C2 indicate that, 

although drilling may have induced changes in the 

ground-water system, these changes were relatively 

small in terms of the absolute value of the pre-drilling 

water level.

Displacement of Water by the Drill Rod

Another stress imposed in the test holes during 

drilling and measurement of water levels was the displacement of water caused by the drill string itself. For 

the most part, water levels were measured inside the 

drill rod after lowering the drill string into the hole each 

morning. The core bit usually was at the bottom of the 

hole or within a foot or so of the bottom when the water 

level inside the drill rod was measured. The diameter of 

the test holes was l-l/2 in. whereas the outside and 

inside diameters of the drill rod were l-5/i6 and 7/g in. 

respectively. As a result, the drill string occupied about 

42 percent of the volume of the hole and would have 

displaced a significant amount of water in the hole, at 

least initially.

The displacement by the drill string would create 

a potential difference between pre-drilling water levels 

in the vicinity of the test hole and those measured during drilling by an amount dependent on the height of 

the initial displacement, the hydraulic properties of the 

aquifer, the diameter of the test hole, and the length of 

time the drill string had been in the hole at the time the

water level was measured. Ultimately, given sufficient 

time, the water level inside the hole would decline to its 

value before the drill rod was inserted.

The time, t, required for water levels to return to 

approximate pre-insertion values after insertion of the 

drill string was estimated using the methodology 

described by Cooper and others (1967) (table C3). This 

technique assumes that (1) the displacement of water 

by the drill string is equivalent to an instantaneous 

"slug" of water of the same volume as the drill string; 

and (2) the hydraulic conductivity of the aquifer is 

about 1 ft/d and the transmissivity equals the hydraulic 

conductivity of the aquifer times the depth of water in 

the hole. The methodology described by Cooper and 

others (1967) is strictly applicable only to fully penetrating wells in confined aquifers of low transmissivity. 

It can be used in other conditions, such as those 

described for the Nahiku area, only to make approximate estimates. As shown in table C3, estimated values 

for t are made for depths of water in the hole of 200, 

100, and 10 ft. The times required for water levels to 

return to pre-insertion values are 0.28, 0.56, and 5.6 

minutes respectively.

Although the times shown in table C3 represent 

approximate times necessary for water levels to return 

to their pre-insertion levels, they are sufficiently low to 

indicate that the effect of the displacement of water by 

the drill string on water levels in the test hole was 

essentially dissipated within a few minutes or less, 

given the general depth of water in the hole as depicted 

in figure 17. Because the drill string was not instantly 

lowered to the bottom of the hole it would appear that 

the difference between the water level in the well 

before insertion of the drill rod and following its insertion probably was negligible at the time of the waterlevel measurements.

This conclusion is further supported by a test 

done by the driller on test hole 85 to estimate the static 

water level at a depth of 712 ft in the hole. The water 

level inside a 1-in. pipe, perforated on the bottom 60 ft, 

was measured before directing a stream of water 

"amounting to about 7 gpm' [gal/min], into the pipe for 

a few minutes, after which a measurement was again 

made which established the water level at the same 

elevation" (J.M. Heizer, 1941, unpub. driller's notes, in 

files of U.S. Geological Survey, Honolulu).

Perhaps the most significant data with regard to 

assessing the potential effect of the displacement of 

water in the test holes by the drill rod are the water levels measured in the 12 test holes completed in the

64 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
Table C2. Altitude of water level in selected test holes for selected times, Nahiku area, Maui, Hawaii

[--, no data; datum is mean sea level. Data from unpub. well logs in files at U.S. Geological Survey, Honolulu]

Altitude of the water level 

(feet)

Date

Mar. 21, 1941

Apr. 12, 1941

Apr. 17, 1941

Apr. 28, 1941

May 29, 1941

May 31, 1941

Mar. 5, 1943

June 21, 1943

June 23, 1943

test hole 74

—

-

-

-

1 827.4

827.7

848.2

-

835.2

test hole 83

! 806.8

--

805.9

803.7

802.0

--

815.9

816.4

813.7

test hole 85

—

^30

830.9

830.1

823.4

--

831.1

--

831.4

1 Water level at end of drilling

Table C3. Estimated time, t, for water levels to decline to 

pre-drill-rod insertion values, following drill-rod insertion, 

Nahiku area, Maui, Hawaii

Depth of water in the test hole 

(feet)

200 

100 

10

t 

(minutes)

0.28 

0.56 

5.6

Honomanu Basalt by methods other than from inside 

the drill rod. Water levels in these holes were always 

higher than those measured from inside the drill rod 

with the bit at the bottom of the hole. In those holes 

where the drill rod (or pipe) was raised, the depth to 

water decreased. This is exactly the opposite of what 

would occur if displacement of water by the drill rod 

was a major factor with regard to the water level in the 

boreholes.

Movement of Water in the Open Test Hole

For most, if not all of their depths, the test holes 

were uncased while drilling was in progress and afterwards. Water is free to move in an open hole in saturated rock from areas of high head to areas of low head, 

where perched water exists, from the perched water 

body down the hole. The effect of movement on the 

water level in a hole is potentially significant in that the 

altitude of the water level in the hole would be expected 

to change over some unknown time period.

In a perched ground-water system, water moving 

down a hole could cause water to be detected in the 

hole when, in fact, the hole was being drilled in 

unsaturated rock. Even so, the altitude of the water

level in the hole would generally decline with increasing hole depth. In a saturated ground-water system 

where the general movement of water is downward, the 

movement of water down the hole would be expected 

to increase the altitude of the water level in the hole 

compared to the pre-drilling hydraulic head at any 

given depth. If the movement of water is upward, the 

altitude of the water level in the borehole would also be 

greater than the pre-drilling hydraulic head at a given 

depth of the hole. The magnitude of the head change 

above the pre-drilling head at any given depth would 

depend on the rate of water movement in the hole, the 

time over which the movement of water existed, and 

the hydraulic properties of the rock within which water 

is moving. It is clear from the directional current-meter 

data collected in some of the boreholes that water was 

moving vertically in at least some of the test holes. It is 

also clear from the driller's log that water was cascading downward in some of the holes.

The potential effect of cascading water on the 

altitude of water levels in the test holes is somewhat 

difficult to completely address. Cascading water was 

reported in about 30 percent of the holes completed in 

the Hana or the Kula Volcanics. On the one hand, cascading water could cause water levels in a given hole to 

be greater than they would be otherwise. On the other 

hand, the data indicate that cascading water was generally associated with large declines in the water level in 

the test holes. These declines generally occurred during 

drilling at zones where drilling pressure was lost over 

small vertical distances (generally several inches or 

so). These large losses in water level in the test holes, 

in turn, resulted in cascading water from zones above 

the new water level in the hole and below the previous

Appendix C: Effect of Drilling on Water-Level Measurements 65
water level. The latter phenomena could occur in either 

a succession of perched water bodies or in a fully saturated anisotropic ground-water system where heads 

decline with depth.

Previous work in the area concluded that the 

Hana Volcanics was unsaturated and the lavas of the 

Kula Volcanics and the rocks of Honomanu Basalt 

were considered to be too permeable to perch water 

outside of the artesian water body (Stearns and Macdonald, 1942). Ground water in the area was considered to occur as perched water bodies in the Kula 

Volcanics, as two artesian water bodies of limited areal 

extent in the upper part of the Honomanu Basalt, and as 

a basal water body with water levels of 10 ft or less in 

the Honomanu Basalt. Although the Kula Volcanics 

was considered too permeable to perch water, Stearns 

and Macdonald (1942, p. 86) state that "when viewed 

as a unit, the Kula contains enough more or less impermeable layers, even though discontinuous, to retard 

greatly the downward percolation of water in areas 

where 100 to 400 inches of rain falls annually [such as 

in the Nahiku area]." The Stearns and Macdonald 

(1942) description of ground-water occurrence indicates that cascading water should occur only after the 

Kula Volcanics had been penetrated.

The presence of water in the Hana Volcanics in 

all of the test holes and water levels significantly above 

the Kula Volcanics in most of the holes clearly cannot 

be the result of cascading water from the underlying 

Kula Volcanics. Even if the water levels in the boreholes are to some extent the result of cascading water 

within the Hana Volcanics, it is still clear from the data 

that there is a considerable amount of water in the Hana 

Volcanics. Because water was initially encountered at 

shallow depths in the test holes, it is doubtful that cascading water, if present, had any significant effect on 

the altitude of the first water encountered in the borehole.

The continual presence of water above the top of 

the Kula Volcanics for hole depths into the Honomanu 

Basalt (including depths far below sea level) for the 

majority of the boreholes also makes it difficult to 

explain the presence of water in the holes solely as a 

product of cascading water from the Kula Volcanics. 

Instead, the continual presence of water above the Kula 

Volcanics in many of the test holes as they were deepened from the Hana Volcanics into the Honomanu 

Basalt indicates that either: (1) the rocks are saturated 

from the Hana Volcanics on down, or (2) that numerous 

perched water bodies occur throughout the stratigraphic column from the Hana Volcanics to the Honomanu Basalt and that cascading water from these 

perched water bodies maintains the water level in the 

borehole above the Kula Volcanics. On the basis of 

stratigraphic knowledge alone, the presence of numerous water bodies in the Hana Volcanics and the Honomanu Basalt is difficult to justify.

Several other factors indicate that cascading 

water may have not played a significant role in the 

water levels in some of the test holes. Surface casing 

was installed in some of the test holes including test 

holes 34, 35,41, and 81. The water level in these holes 

remained above the bottom of the casing and above the 

top of the Kula Volcanics as the holes were deepened 

from the Hana Volcanics into the Kula Volcanics and, 

at test hole 81, into the Honomanu Basalt. It is safe to 

assume that cascading water played no role in the water 

levels in these holes. These data indicate that the rocks 

of the Hana and Kula Volcanics are saturated below the 

first water encountered during drilling. Water-level 

data from other nearby test holes are similar to waterlevel data in test holes 34, 35, 41, and 81 even though 

water levels in these holes either fell below the casing 

or no casing was reported.

If cascading water was responsible for maintaining water in the test hole at the end of the day's drilling, 

then the rate of cascading water would have to have 

been sufficient to establish and maintain hundreds of 

feet of water in the holes (fig. 9). This would, in turn, 

cause the altitude of the water level in the well to continue to increase overnight or for a period of several 

days or more in the continued absence of drilling and in 

the continued presence of cascading water until equilibrium was reached. The available data (tables Cl and 

C2) do not support this. The maximum difference 

between water levels measured at the end of a day's 

drilling and those measured 1 to 3 days before the 

resumption of drilling was 4 ft, although identical measurements were more common. The maximum change 

after 1 to 2 months was 6.6 ft. The maximum change in 

water levels following completion of drilling that was 

observed after more than 2 years was 20.5 ft. The latter 

measurements were only made during March and June 

over the 2-year span and are, therefore, not necessarily 

indicative of the greatest change over the 2-year time 

period. Because they were made during the same 

months of each year, however, the measurements are 

still comparable.

The directional current-meter data also indicate 

that the effect of cascading water on the overall profile

66 A Reevaluation of the Occurrence of Ground Water in the Nahiku Area, East Maui, Hawaii
of water levels in at least sc tie of the boreholes was not 

significant. This is indicate by the fact that the direction of water movement in tt >se holes where these data 

were obtained is in accord \\ th the water levels measured in the holes as drilling Drogressed.

Several test holes beaj special mention with 

regard to what was apparent y a major movement of 

water down the hole. As she vn in table 5, no water was 

in T-86 at a hole depth of 5 2 ft. Before this, the water 

level measured inside the < rill rod at a hole depth of 

496 ft stood 173 ft above le bottom of the hole. 

Between the hole depths < f 496 and 552 ft, the driller 

reported "heavy leaks" at depths of 500, 510, and 552 

ft. Water was reported in :he hole at hole depths below 

552 ft, but the depth to ^ ater in the hole ranged from 

546 to 621 ft. As noted i appendix A, at the final hole 

depth of 817 ft, depth tc water measured inside the drill 

rod was 614 ft and din ;tional current-meter measurements made foliowim :he completion of the hole indicated water at a dep'/> )f only 180 ft.

The complf / 1 ss of water in test hole 86 at a 

depth of 552 ft r'.* j. nc happen in any other test hole 

once water w? , ^nco ntered although it nearly 

occurred at t' ',t hole 52. Given that once water was 

encountered m th', other test holes it remained in the 

holes, the omplete loss of water in test hole 86 was

probably in response to some localized condition such 

as a partially saturated lava tube.

The altitude of the water level in test hole 62 fell 

from 1,071 ft, at a bottom hole altitude of 804 ft, to 773 

ft, at a bottom hole altitude of 770 ft (table 5). The 

height of water fell from 267 to 3 ft above the bottom 

of the hole. The test hole was deepened 16 ft and the 

water level rose 82 ft. At this point the height of water 

was 85 ft above the bottom of the hole. The altitude of 

the water level and the height of water above the bottom of the hole generally tended to increase from this 

point on. Ultimately, the altitude of the water level in 

the well was 1,212 ft for a bottom hole altitude of 380 

ft. This corresponds to a water level of 832 ft above the 

bottom of the hole.

The situation at test hole 62 was sufficiently rare 

as to receive a comment from the driller. As reported in 

the driller's log: "With reference to the low water levels 

found at 425 and 625 [bottom hole altitude of 770 ft] it 

is occasionally observed that a freak low level is found 

in the course of drilling which may be accounted for by 

the assumption that an area may have been cut into, 

which, until it has been filled with water, may temporarily lower the water in the hole, and which, after 

being filled, permitting the water to again rise in the 

hole, may give the impression of an artesian movement."

Appendix C: Effect of Drilling on Water-Level Measurements 67
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii

[Values in feet; --, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in f

3

(D

oo 

o

a

o

I

a

CO 

<D

Land _ . Depth to top Depth to Vertical .. , 

surface '""' of Kula base of Kula hydraulic "°'e. 

altitude aepin Volcanics Volcanics gradient aeptn

Bottom 

hole 

altitude

Depth to 

water

Water-level 

altitude

Water level 

above top Rock 

of Kula unit1 

Volcanics

Test hole 12

1,282 937 164 636 0.82 38

99

104

342

386

421

443

452

470

489

525

561

599

620

657

687

713

736

759

800

806 

806

830

865

874

915

937

1,244

1,183

1,178

940

896

861

839

830

812

793

757

721

683

662

625

595

569

546

523

482

476 

476

452

417

408

367

345

35

37

37

123

123

125

141

139

155

236

268

335

318

328

310

346

342

344

345

510

508 

2200

503

493

498

535

774

1,247

1,245

1,245

1,159

1,159

1,157

1,141

1,143

1,127

1,046

1,014

947

964

954

972

936

940

938

937

772

774 

1,082

779

789

784

747

508

129 Hana

127 Hana

127 Hana

41 Kula

41 Kula

39 Kula

23 Kula

25 Kula

9 Kula

-72 Kula

-104 Kula

-171 Kula

-154 Kula

-164 Kula

-146 Honomanu

-182 Honomanu

-178 Honomanu

-180 Honomanu

-181 Honomanu

-346 Honomanu

-344 Honomanu 

-36 Honomanu

-339 Honomanu

-329 Honomanu

-334 Honomanu

-37 1 Honomanu

-610 Honomanu

Test hole 62

60

79

153

362

452

482

489

516

559

592

625

641

667

680

1,335

1,316

1,242

1,033

943

913

906

879

836

803

770

754

728

715

37

73

91

243

263

238

238

251

289

324

622

556

529

515

1,358

1,322

1,304

1,152

1,132

1,157

1,157

1,144

1,106

1,071

773

839

866

880

188 Hana

152 Hana

134 Hana

-18 Kula

-38 Kula

-13 Honomanu

-13 Honomanu

-26 Honomanu

-64 Honomanu

-99 Honomanu

-397 Honomanu

-331 Honomanu

-304 Honomanu

-290 Honomanu
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; --, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

Land Tt . Depth to top Depth to Vertical H . 

surface ' OIfh of Kula base of Kula hydraulic "~J? 

altitude aepin Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to 

water

Water level 

Water-level above top Rock 

a,titude of Kula unit' 

Volcanics

Test hole 62-Continued

691

727

751

766

780

814

829

862

881

900

921

948

954

976

977

988

994

997

1,001

704

668

644

629

615

581

566

533

514

495

474

447

441

419

418

407

401

398

394

605

609

611

606

607

605

602

605

603

597

603

580

567

591

418

373

562

275

293/3 281

790

786

784

789

788

790

793

790

792

798

792

815

828

804

977

1,022

833

1,120

1,102/1,114

-380

-384

-386

-381

-382

-380

-377

-380

-378

-372

-378

-355

-342

-366

-193

-148

-337

-50

-687-56

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 65

1,066 642 218 452 0.68 18

140

152

184

218

236

332

395

409

498

529

529

1,048

926

914

882

848

830

734

671

657

568

537

537

15

93

90

92

107

109

112

121

121

141

362

4 184

1,051

973

976

974

959

957

954

945

945

925

704

882

203

125

128

126

111

109

106

97

97

77

-144

34

Hana

Hana

Hana

Hana

Hana/Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Test hole 74

1,072 632 227 460 0.32 131

140

154

191

199

228

247

941

932

918

881

873

844

825

83

105

116

120

120

120

120

989

967

956

952

952

952

952

144

122

111

107

107

107

107

Hana

Hana

Hana

Hana

Hana

Kula/Hana

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

(D

o

o 

o

I

8

o

I

a 

I

m 

o>

(0 

B>

c

Q>

I

Land _ . . Depth to top Depth to Vertical H . 

surface '°T;J. of Kula base of Kula hydraulic "oie. 

altitude aep Volcanics Volcanics gradient eptn

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

Water level 

» » 

Volcanics

Test hole 74-Continued

280

322

503

549

576

587

591

601

606

621

632

792

750

569

523

496

485

481

471

466

451

440

120

120

372

374

358

287

265

259

248

245

244

952

952

700

698

714

785

807

813

824

827

828

107

107

-145

-147

-131

-60

-38

-32

-21

-18

-17

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 81

984 521 192 453 0.03 176

231

282

314

386

469

479

521

808

753

702

670

598

515

505

463

10

12

11

11

11

14

18

20

974

972

973

973

973

970

966

964

182

180

181

181

181

178

174

172

Hana

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Test hole 82

924 478 195 434 0.67 60

71

158

181

211

251

257

304

345

348

371

384

394

450

468

478

864

853

766

743

713

673

667

620

579

576

553

540

530

474

456

446

-

61

110

118

124

122

124

179

179

181

185

185

205

326

327

--

-

863

814

806

800

802

800

745

745

743

739

739

719

598

597

-

-

134

85

77

71

73

71

16

16

14

10

10

-10

-131

-132

-

Hana

Hana

Hana

Hana

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Test hole 83

945 790 173 447 0.97 170

340

775

605

106

124

839

821

67

49

Hana

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

Land T . . Depth to top Depth to Vertical H . 

surface !TMJ' of Kula base of Kula hydraulic "°J? 

altitude aeptn Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

Water level 

ab??!°P "So 

o Kua unit' 

Volcanics

Test hole 83-Continued

384

405

448

519

575

664

696

721

777

790 

790

561

540

497

426

370

281

249

224

168

155 

155

129

287

345

242

120

123

123

123

122

709 

2230

816

658

600

703

825

822

822

822

823

236 

2715

44

-114

-172

-69

53

50

50

50

51

-536

2-57

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Test hole 84

977 441 187 430 0.05 65

67

99

121

209

304

318

335

377

386

427

441

912

910

878

856

768

673

659

642

600

591

550

536

36

45

58

63

47

45

45

47

49

50

50

56

941

932

919

914

930

932

932

930

928

927

927

921

151

142

129

124

140

142

142

140

138

137

137

131

Hana

Hana

Hana

Hana

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Test hole 85

1,003 991 226 543 0.66 45

95

146

256

284

318

360

393

436

465

489

505

514

517

521

958

908

857

747

719

685

643

610

567

538

514

498

489

486

482

44

48

50

50

50

50

50

47

44

48

57

57

58

104

103

959

955

953

953

953

953

953

956

959

955

946

946

945

899

900

182

178

176

176

176

176

176

179

182

178

169

169

168

122

123

Hana

Hana

Hana

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in files 

<D

O 

o 

o

8 

a

o 

o

Q.

CD 

<D

3

r*

<D 

CD

Land _ t . Depth to top Depth to Vertical .. . 

surface 1;TM?' of Kula base of Kula hydraulic "°ieh 

altitude p Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

Water level 

above top Rock 

oKula umt1 

Volcanics

Test hole 85-Continued

554

658

865

900

934

951

991 

991

449

345

138

103

69

52

12 

12

103

104

176

250

475

424

666

5 173

900

899

827

753

528

579

337 

830

123

122

50

-24

-249

-198

-440 

53

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Test hole 86

1,494 817 243 584 0.76 191 

203 

246 

282

296

496

552

559

606

635

676

711

756

782

800

817 

817

1,303 

1,291 

1,248 

1,212

1,198

998

942

935

888

859

818

783

738

712

694

677 

677

°139 

6 141 

6 137 

6 140

6140

323

no water

556

549

546

554

546

616

616

621

614 

2 180

1,355 

1,353 

1,357 

1,354

1,354

1,171

-

938

945

948

940

948

878

878

873

880 

1,314

104 

102 

106 

103

103

-80

-

-313

-306

-303

-311

-303

-373

-373

-378

-371 

63

Hana 

Hana 

Kula 

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Test hole 87

465 738 258 426 0.60 194

356

502

522

530

540

558

575

600 

609

615

623

639

271

109

-37

-57

-65

-75

-93

-110

-135 

-144

-150

-158

-174

90

83

102

102

103

103

104

104

105 

795

136

128

108

375

382

363

363

362

362

361

361

360 

370

329

337

357

168

175

156

156

155

155

154

154

153 

163

122

130

150

Hana

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Honomanu

Honomanu

Honomanu
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; --, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in fi

Land T . , Depth to top Depth to Vertical H , 

surface ! T J, of Kula base of Kula hydraulic "Ol® 

altitude ep Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

Water level 

above top Rock 

o Kula umt1 

Volcanics

Test hole 87-Continued

655

666

690

707

724

732

738

738

-190

-201

-225

-242

-259

-267

-273

-273

124

124

193

189

189

415

415

8 105

341

341

272

276

276

50

50

360

134

134

65

69

69

-157

-157

153

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 88

135 475 85 225 0.10 166

181

198

208

232

251

262

279

302

309

325

335

346

365

382

403

411

423

448

475

-31

-46

-63

-73

-97

-116

-127

-144

-167

-174

-190

-200

-211

-230

-247

-268

-276

-288

-313

-340

88

87

87

81

75

76

73

83

83

64

77

92

92

93

94

94

101

121

121

119

47

48

48

54

60

59

62

52

52

71

58

43

43

42

41

41

34

14

14

16

-3

-2

-2

4

10

9

12

2

2

21

8

-7

-7

-8

-9

-9

-16

-36

-36

-34

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 89

449 587 183 290 0.51 137

216

231

245

296

320

337

375

401

312

233

218

204

153

129

112

74

48

109

109

109

111

111

121

128

139

228

340

340

340

338

338

328

321

310

221

74

74

74

72

72

62

55

44

-45

Hana

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in fil

<D 

O 

§

|

8 

O

Land _ . Depth to top Depth to Vertical H .

surface Honth of Kula base of Kula hydraulic Honth 

altitude epl Volcanics Volcanics gradient epin

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

Water level 

ab°ve top R°?f 

o Kula un.t1 

Volcanics

Test hole 89-Continued

415

442

455

507

530

548

568

581

34

7

-6

-58

-81

-99

-119

-132

223

222

227

227

228

231

339

334

226

227

222

222

221

218

110

115

-40

-39

-44

-44

-45

-48

-156

-151

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 90

864 847 441 604 0.42 181

191

262

282

308

339

371

413

465

480

486

496

499

512

530

605

661

674

687

767

811

847 

847

683

673

602

582

556

525

493-

451

399

384

378

368

365

352

334

259

203

190

177

97

53

17

17

131

131

213

232

232

230

223

232

232

248

248

241

235

403

407

406

408

422

410

412

411

411 

9240

733

733

651

632

632

634

641

632

632

616

616

623

629

461

457

458

456

442

454

452

453

453 

624

310

310

228

209

209

211

218

209

209

193

193

200

206

38

34

35

33

19

31

29

30

30 

201

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Test hole 91

762 548 205 385 0.25 184

207

209

242

280

302

322

578

555

553

520

482

460

440

106

107

110

132

126

124

149

656

655

652

630

636

638

613

99

98

95

73

79

81

56

Hana

Kula

Kula

Kula

Kula

Kula

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in fi

Land _. . Depth to top Depth to Vertical H . 

surface !!"?' of Kula base of Kula hydraulic P°J? 

altitude ep Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

?6 ?Ve' D „ 

above op Rock 

o Kula umt1 

Volcanics

Test hole 91 -Continued

342

390

430

465

476

486

530

548

420

372

332

297

286

276

232

214

127

148

162

222

198

201

201

198

635

614

600

540

564

561

561

564

78

57

43

-17

7

4

4

7

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 92

902 754 211 442 0.77 131

136 

199

226

351

392

401

413

423

449

467

481

502

519

547

572

687

707

745

754 

754

771

766 

703

676

551

510

501

489

479

453

435

421

400

383

355

330

215

195

157

148 

148

81

70 

10 171

172

206

180

177

300

296

273

222

157

157

157

83

85

85

82

85

561 

H 86

821

832 

731

730

696

722

725

602

606

629

680

745

745

745

819

817

817

820

817

341 

816

130

141 

40

39

5

31

34

-89

-85

-62

-11

54

54

54

128

126

126

129

126

-350 

125

Hana

Hana 

Hana

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Test hole 93

849 614 186 440 -0.06 155

180

267

271

277

312

374

405

432

694

669

582

578

572

537

475

444

417

105

125

125

127

183

124

126

127

128

744

724

724

722

666

725

723

722

721

81

61

61

59

3

62

60

59

58

Hana

Hana

Kula

Kula

Kula

Kula

Kula

Kula

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; --, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in fil

(D

O

(D

£

O 

5

5T

Land T t , Depth to top Depth to Vertical H . 

surface . ° ?' of Kula base of Kula hydraulic "° th 

altitude aepin Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Water level 

Depth to Water-level above top Rock 

water altitude of Kula mitt' 

Volcanics

Test hole 93-Continued

452

476

492

509

533

554

597

602

614

397

373

357

340

316

295

252

247

235

129

109

92

83

66

48

47

46

78

720

740

757

766

783

801

802

803

771

57

77

94

103

120

138

139

140

108

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 94

796 649 182 405 -0.20 352

394

408

411

439

456

460

482

494

536

555

575

596

596

596

603

617

634

649

444

402

388

385

357

340

336

314

302

260

241

221

200

200

200

193

179

162

147

189

215

210

203

174

182

153

114

109

277

96

134

*98

130

132

136

135

134

130

607

581

586

593

622

614

643

682

687

719

700

662

698

666

664

660

661

662

666

-7

-33

-28

-21

8

0

29

68

73

105

86

48

84

52

50

46

47

48

52

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Hana

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 96

785 530 195 401 0.21 284

305

314

332

341

371

398

430

469

482

501

480

471

453

444

414

387

355

316

303

87

103

95

97

88

98

96

106

104

103

698

682

690

688

697

687

689

679

681

682

108

92

100

98

107

97

99

89

91

92

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; --, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

Land _. . Depth to top Depth to Vertical „ . 

surface ' fj, of Kula base of Kula hydraulic "Ol® 

altitude a p Volcanics Volcanics gradient aeptn

Bottom 

hole 

altitude

Water level 

Depth to Water-level above top Rock 

water ,,,,,ude o| Kula" un,,' 

Volcanics

Test hole 96-Continued

491

501

520

294

284

265

107

130

137

678

655

648

88

65

58

Honomanu

Honomanu

Honomanu

Test hole 97

826 595 300 363 0.51 107 

141 

162

192

202

214

233

257

273

283

286

302

308

430

465

473

495

505 

508

517

526

546 

561

595 

595

719 

685 

664

634

624

612

593

569

553

543

540

524

518

396

361

353

331

321 

318

309

300

280 

265

231 

231

1Z96

12 123 

12 132

129

131

135

134

143

132

145

146

146

154

145

165

347

340

352 

12 174

317

343

346 

13 348

345 

2298

730 

703 

694

697

695

691

692

683

694

681

680

680

672

681

661

479

486

474 

652

509

483

480 

478

481 

528

204 

177 

168

171

169

165

166

157

168

155

154

154

146

155

135

-47

-40

-52 

126

-17

-43

-46 

-48

-45

2

Hana 

Hana 

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Hana

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Honomanu

Honomanu

Honomanu 

Honomanu

Honomanu 

Honomanu

Test hole 98

1,015 755 241 528 0.42 141

182

196 

211

222

238

242

257

285

301

874

833

819 

804

793

111

773

758

730

714

91

158

156 

14 159

199

199

201

202

261

261

924

857

859 

856

816

816

814

813

754

754

150

83

85 

82

42

42

40

39

-20

-20

Hana

Hana

Hana 

Hana

Hana

Hana

Kula

Kula

Kula

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; —, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

** Land T . Depth to top 

» surface !°JJ' of Kula 

? altitude depth Volcanics

SL

Si

o

3

"^

(B

O 

o

0

i

i(D

a

o

5

c

3

Q.

I

5'

5

(B

z

3"

•f

C

3

a>

g2.

a>

c.

|TM

Depth to Vertical ,. , 

base of Kula hydraulic .M°'e 

Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to 

water

Water-level 

altitude

Water level 

above op Rock 

o Kula umt1 

Volcanics

Test hole 98-Continued

306

318

335

352

355

388

405

415

430

450

468

483

500

520

534

542

549

555

563

580

600

620

638

648

662

680

688

700

712

725

733

750

755

709

697

680

663

660

627

610

600

585

565

547

532

515

495

481

473

466

460

452

435

415

395

377

367

353

335

327

315

303

290

282

265

260

261

262

260

257

257

258

260

259

258

258

256

318

265

305

295

302

306

300

273

316

310

366

315

315

320

330

395

339

15 330

323

337

361

349

754

753

755

758

758

757

755

756

757

757

759

697

750

710

720

713

709

715

742

699

705

649

700

700

695

685

620

676

685

692

678

654

666

-20

-21

-19

-16

-16

-17

-19

-18

-17

-17

-15

-77

-24

-64

-54

-61

-65

-59

-32

-75

-69

-125

-74

-74

-79

-89

-154

-98

-89

-82

-96

-120

-108

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 99

1,578 1,030 191 687 0.32 184

200

216

224

229

239

1,394

1,378

1,362

1,354

1,349

1,339

174

182

181

182

182

182

1,404

1,396

1,397

1,396

1,396

1,396

17

9

10

9

9

9

Hana

Kula

Kula

Kula

Kula

Kula
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; -, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

Land T t , Depth to top Depth to Vertical H . 

surface !°,' of Kula base of Kula hydraulic "°'e. 

altitude aep Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to 

water

Water-level 

altitude

Water level 

above top Rock 

of Kula unit1 

Volcanics

Test hole 99-Continued

250

261

272

280

300

315

328

335

353

363

377 

393

406

419

434

448

472

494

501

515

525

535

547

555

566

578

584

602

611

616

620

624

633

639

655

662

674

685

705

713

1,328

1,317

1,306

1,298

1,278

1,263

1,250

1,243

1,225

1,215

1,201 

1,185

1,172

1,159

1,144

1,130

1,106

1,084

1,077

1,063

1,053

1,043

1,031

1,023

1,012

1,000

994

976

967

962

958

954

945

939

923

916

904

893

873

865

182

213

191

189

188

189

192

189

199

206

211 

345/16305

327

322

305

315

342

472

472

463

456

489

533

533

558

551

551

585

595

594

600

605

615

620

635

640

650

665

675

676

1,396

1,365

1,387

1,389

1,390

1,389

1,386

1,389

1,379

1,372

1,367 

1,233/1,273

1,251

1,256

1,273

1,263

1,236

1,106

1,106

1,115

1,122

1,089

1,045

1,045

1,020

1,027

1,027

993

983

984

978

973

963

958

943

938

928

913

903

902

9 Kula

-22 Kula

0 Kula

2 Kula

3 Kula

2 Kula

-1 Kula

2 Kula

-8 Kula

-15 Kula

-20 Kula 

-154/-114 Kula

-136 Kula

-131 Kula

-114 Kula

-124 Kula

-151 Kula

-281 Kula

-281 Kula

-272 Kula

-265 Kula

-298 Kula

-342 Kula

-342 Kula

-367 Kula

-360 Kula

-360 Kula

-394 Kula

-404 Kula

-403 Kula

-409 Kula

-414 Kula

-424 Kula

-429 Kula

-444 Kula

-449 Kula

-459 Kula

-474 Kula

-484 Honomanu

-485 Honomanu
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; -, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in file

^ Land T0tai Depth to top Depth to 

o surface . ° .. of Kula base of Kula

% altitude a ptn Volcanics Volcanics

so

»

o

3

ar*

3-

O 

o

o

§o

a

O ——————————————————————————————————

S

g 1,845 1,132 362 1,060

a

o>

55'

r*

z

0>

c

1J»

mo>

a

o>

c_

I—

Vertical „ . 

hydraulic ri"°'eh 

gradient depth

Bottom 

hole 

altitude

Depth to Water-level 

water altitude

Water level 

above top Rock 

o Kula unit1 

Volcanics

Test hole 99-Continued

720

731

945

950

990

998

1,015

1,024

1,024

1,030

858

847

633

628

588

580

563

554

554

548

700

710

456

454

454

458

448

451

2385

447

878

868

1,122

1,124

1,124

1,120

1,120

1,127

1,193

1,131

-509

-519

-265

-263

-263

-267

-257

-260

-194

-256

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Honomanu

Test hole 100

0.46 596

646

666

685

694

709

725

730

734

749

765

774

789

796

821

829

841

851

861

931

946

967

979

991

1,007

1,032

1,061

1,072

1,072

1,249

1,199

1,179

1,160

1,151

1,136

1,120

1,115

1,111

1,096

1,080

1,071

1,056

1,049

1,024

1,016

1,004

994

984

914

899

878

866

854

838

813

784

773

773

449

492

559

555

675

690

705

710

715

730

745

755

770

739

716

715

719

716

715

711

671

675

675

675

666

666

666

669

2400

1,396

1,353

1,286

1,290

1,170

1,155

1,140

1,135

1,130

1,115

1,100

1,090

1,075

1,106

1,129

1,130

1,126

1,129

1,130

1,134

1,174

1,170

1,170

1,170

1,179

1,179

1,179

1,176

1,445

-87

-130

-197

-193

-313

-328

-343

-348

-353

-368

-383

-393

-408

-377

-354

-353

-357

-354

-353

-349

-309

-313

-313

-313

-304

-304

-304

-307

-38

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Kula

Honomanu

Honomanu

Honomanu
Table 5. Water levels in selected test holes completed in Honomanu Basalt, Nahiku area, Maui, Hawaii-Continued

[Values in feet; --, no data or not applicable; Kula, Kula Volcanics; Hana, Hana Volcanics; Honomanu, Honomanu Basalt. Data from unpub. well logs in fi

Land T . Depth to top Depth to Vertical H , 

surface . ,' of Kula base of Kula hydraulic ",. 

altitude aepin Volcanics Volcanics gradient aepin

Bottom 

hole 

altitude

Depth to 

water

Water-level 

altitude

Water level 

above top Rock 

of Kula unit1 

Volcanics

Test hole 100-Continued

1,120

1,132

725

713

734

695

1,111

1,150

-372 . Honomanu

-333 Honomanu

Kuhiwa well

1,396 1,405 258 744 0.02 954

961

982

1,012

1,095

1,110

1,122

1,175

1,188

1,210

1,229

1,245

1,248

1,256

1,328

1,360

1,405

442

435

414

384

301

286

274

221

208

186

167

151

148

140

68

36

-9

260

243

246

256

259

259

250

245

236

249

253

253

256

267

309

317

270

1,136

1,153

1,150

1,140

1,137

1,138

1,146

1,151

1,160

1,147

1,143

1,143

1,140

1,129

1,087

1,079

1,126

-2 Honomanu

15 Honomanu

12 Honomanu

2 Honomanu

- 1 Honomanu

0 Honomanu

8 Honomanu

13 Honomanu

22 Honomanu

9 Honomanu

5 Honomanu

5 Honomanu

2 Honomanu

-9 Honomanu

-5 1 Honomanu

-59 Honomanu

-12 Honomanu

Based on unpublished geologic logs in files at USGS, Honolulu District office 

Current-meter reading

3 Depth to water after 17 hours, no water pumped in hole

4 Raised pipe in hole; pipe at hole depth of 190 feet

5 Raised pipe to a depth of 791 feet

Measurement made by air pressure in drilling rods 

Measurement made with drill bit at a depth of 348 feet

8 Measurement made with drill bit at a depth of 175 feet

9 Drill bit raised to a hole depth of 300 feet

Measurement made at a drill bit depth of 194 feet 

Measurement made at a drill bit depth of 649 feet 

Measurement made with air in drill column

13 Raised pipe in hole to a depth of 519 feet

14 Raised pipe in hole to a depth of 199 feet

15 Raised pipe in hole to a depth of 700 feet

Water level dropped to 345 feet, gradually rose to 305 feet

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