Ground Displacements Caused by AquiferSystem Water-Level Variations Observed Using

Interferometric Synthetic Aperture Radar near

Albuquerque, New Mexico

Prepared in cooperation with the

CITY OF ALBUQUERQUE

U.S. Department of the Interior

U.S. Geological Survey

Water-Resources Investigations Report 02-4235
U.S. GEOLOGICAL SURVEY

Water-Resources Investigations Report 02-4235

Ground Displacements Caused by AquiferSystem Water-Level Variations Observed Using

Interferometric Synthetic Aperture Radar near

Albuquerque, New Mexico

Prepared in cooperation with the

CITY OF ALBUQUERQUE

By Charles E. Heywood, Devin L. Galloway, and Sylvia V. Stork

Albuquerque, New Mexico

2002
U.S. DEPARTMENT OF THE INTERIOR

GALE A. NORTON, Secretary

U.S. GEOLOGICAL SURVEY

Charles G. Groat, Director

The use of firm, trade, and brand names in this report is for identification purposes only and does

not constitute endorsement by the U.S. Geological Survey.

For additional information write to: Copies of this report can be purchased

U.S. Geological Survey

Information Services

Box 25286

Denver, CO 80225-0286

District Chief

U.S. Geological Survey

Water Resources Division

5338 Montgomery Blvd. NE, Suite 400

Albuquerque, NM 87109-1311

from:

Information regarding research and data-collection programs of the U.S. Geological Survey is available

on the Internet via the World Wide Web. You may connect to the home page for the New Mexico District

Office using the URL http://nm.water.usgs.gov.
iii

CONTENTS

Page

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

Introduction ........................................................................................................................................................................... 1

Purpose and scope ....................................................................................................................................................... 3

Methods ....................................................................................................................................................................... 3

Acknowledgments ....................................................................................................................................................... 3

Radar interferometry.............................................................................................................................................................. 3

Ground-displacement observations ....................................................................................................................................... 4

793-day interferogram (July 2, 1993 - September 3, 1995) ........................................................................................ 4

Rio Rancho ........................................................................................................................................................ 4

Albuquerque ...................................................................................................................................................... 4

211-day interferogram (September 3, 1995 - April 1, 1996)....................................................................................... 12

Rio Rancho ........................................................................................................................................................ 12

Albuquerque ...................................................................................................................................................... 12

1,004-day interferogram (July 2, 1993 - April 1, 1996) .............................................................................................. 12

Rio Rancho ........................................................................................................................................................ 12

Albuquerque ...................................................................................................................................................... 12

385-day interferogram (February 10, 1997 - March 2, 1998) ..................................................................................... 12

Rio Rancho ........................................................................................................................................................ 12

Albuquerque ...................................................................................................................................................... 12

560-day interferogram (March 2, 1998 - September 13, 1999)................................................................................... 12

Rio Rancho ........................................................................................................................................................ 13

Albuquerque ...................................................................................................................................................... 13

Other measurements .................................................................................................................................................... 13

Correlation with ground-water-level changes.............................................................................................................. 13

Geologic structures in the study area that influence ground-water flow ..................................................................... 15

Conclusions ........................................................................................................................................................................... 16

Selected references ................................................................................................................................................................ 16

FIGURES

1. Map showing area of interferogram coverage in the Albuquerque Basin, central New Mexico ............................. 2

2. Maps showing:

A. Interferogram (793 day) showing ground displacement from July 2, 1993, to September 3, 1995 ................... 5

B. Interferogram (211 day) showing ground displacement in relation to mapped faults from September 3,

1995, to April 1, 1996 ........................................................................................................................................ 6

C. Interferogram (1,004 day) showing ground displacement from July 2, 1993, to April 1, 1996 ......................... 7

D. Interferogram (385 day) showing ground displacement from February 10, 1997, to March 2, 1998 ................ 8

E. Interferogram (560 day) showing ground displacement from March 2, 1998, to September 13, 1999.............. 9

3. Graphs showing vertical displacement along profile A-A’ from July 2, 1993, to September 13, 1999................... 10

4. Graphs showing vertical displacement along profile B-B’ from July 2, 1993, to September 13, 1999................... 11

5. Graphs showing depth to water in:

A. Garfield piezometers ........................................................................................................................................... 14

B. Del Sol Divider piezometers ............................................................................................................................... 14

TABLE

1. Selected synthetic aperture radar (SAR) data acquisitions and interferometric pairs.............................................. 3
iv

CONVERSION FACTORS, ABBREVIATIONS, AND DATUMS

Vertical coordinate information is referenced to the North American Vertical Datum of 1988

(NAVD 88).

Horizontal coordinate information is referenced to the North American Vertical Datum of 1983

(NAD 83).

Multiply By To obtain

millimeter (mm) 25.4 inch (in.)

meter (m) 3.281 foot (ft)

kilometer (km) 0.621 mile (mi)

square kilometer (km2) 0.3861 square mile (mi2)

square kilometer (km2) 247.1 acre
1

ABSTRACT

Six synthetic aperture radar (SAR) images were

processed to form five unwrapped interferometric

(InSAR) images of the greater metropolitan area in the

Albuquerque Basin. Most interference patterns in the

images were caused by range displacements resulting

from changes in land-surface elevation. Loci of landsurface elevation changes correlate with changes in

aquifer-system water levels and largely result from the

elastic response of the aquifer-system skeletal material

to changes in pore-fluid pressure. The magnitude of the

observed land-surface subsidence and rebound

suggests that aquifer-system deformation resulting

from ground-water withdrawals in the Albuquerque

area has probably remained in the elastic (recoverable)

range from July 1993 through September 1999.

Evidence of inelastic (permanent) land subsidence in

the Rio Rancho area exists, but its relation to

compaction of the aquifer system is inconclusive

because of insufficient water-level data. Patterns of

elastic deformation in both Albuquerque and Rio

Rancho suggest that intrabasin faults impede groundwater-pressure diffusion at seasonal time scales and

that these faults are probably important in controlling

patterns of regional ground-water flow.

INTRODUCTION

Permanent land subsidence caused by the

inelastic compaction of overdrafted alluvial aquifer

systems is a global problem. In many ground-water

basins in the arid to semiarid Western United States,

permanent regional-scale subsidence has resulted from

mining ground water for agricultural, municipal, and

industrial water supplies (Galloway and others, 1999).

Notable examples are the Antelope (Mojave Desert)

(Ikehara and Phillips, 1994; Galloway and others,

1998; Sneed and Galloway, 2000), Santa Ana (Bawden

and others, 2001), San Joaquin (Poland and others,

1975), and Santa Clara (Poland and Ireland, 1988;

Ikehara and others, 1998) Valleys in California; the Las

Vegas Valley (Bell, 1981a,b; Bell and Price, 1993;

Amelung and others, 1999; Hoffman and others, 2001)

in Nevada; and several basins in south-central Arizona

(Laney and others, 1978; Carpenter, 1999). Presently,

the maximum historical subsidence in these basins

ranges from about 2 to 9 m. In each of these examples,

large volumes of ground water extracted to irrigate

crops and supply municipal-industrial demands caused

ground-water levels to decline below critical

thresholds, leading to the onset of subsidence.

Conjunctive use of local ground-water supplies and

imported surface-water supplies has helped decrease or

halt permanent subsidence in each of these basins.

Short of permanent subsidence, non-permanent,

reversible, elastic deformation occurs in all aquifer

systems subject to pore-fluid-pressure variations. From

other alluvial basins subjected to daily and seasonal

pumping stresses where aquifer-system deformation

has been studied and monitored, we know that these

elastic displacements are typically about 1 mm for

daily periods and can exceed 30–50 mm for seasonal

periods.

In the Albuquerque area, a network of 44

benchmarks was established in 1993, which was

surveyed using the Global Positioning System (GPS) in

March-April 1993 and again in August 1994. In the 16

months between these surveys, no benchmark elevation

changes greater than 1.3 cm were detected, which was

the accuracy limit of the GPS survey technique.

Data collected between December 1994 and

March 2002 at a 315-m-deep borehole extensometer in

the Rio Grande Valley near Albuquerque (Heywood,

1998) indicate that aquifer-system deformation was

predominantly elastic, with less than 2 mm of

permanent compaction over that period. Geomorphic

evidence suggests that the Rio Grande has eroded as

much as 100 m of sediment of Pleistocene age from a

pre-existing fluvial-alluvial plain, of which the present

Llano de Albuquerque (fig. 1) is a relict. Underlying

sediment was preconsolidated by the weight of the

sedimentary overburden; subsequent erosion of the

overburden resulted in overconsolidation of these

sediments. This overconsolidation suggests that

aquifer-system deformation resulting from groundwater-level declines is likely to remain in the elastic

range until such declines cause aquifer-system

GROUND DISPLACEMENTS CAUSED BY AQUIFERSYSTEM WATER-LEVEL VARIATIONS OBSERVED USING

INTERFEROMETRIC SYNTHETIC APERTURE RADAR

NEAR ALBUQUERQUE, NEW MEXICO

By Charles E. Heywood, Devin L. Galloway, and Sylvia V. Stork
2

35°

45 ́

35°

30 ́

35°

15 ́

35°

34°

45 ́

34°

30 ́

34°

15 ́Base compiled from U.S. Geological Survey digital data, 1:100,000

1977, 1978; and City of Albuquerque digital data, 1:2,400, 1994

Figure 1. Area of interferogram coverage in the Albuquerque Basin, central New Mexico.

NEW MEXICO

MAP

AREA

Arroyo

Chico

Rio

Puerco

Rio

Salado

Tijeras

Arroyo

Galisteo

Creek

Arroyo

Tonque Las

tas

Huer

Creek

Bernalillo

107°15 ́ 107° 106°45 ́ 106°30 ́ 106°15 ́

Torrance

Socorro

Bernalillo

Sandoval

Cibola

McKinley

Santa Fe

Rio Rancho

Rio

Grande

San Acacia

Bernardo

Belen

Los Lunas

Rio

Salado

Abo Arroyo

Rio

San

Jose

Isleta

Rio

Puerco

Jemez

Canyon

Reservoir

Albuquerque

Basin

Jemez

River

Cochiti

Lake

Santa

Fe

River

Area of

interferogram

Madrid

Placitas

Golden

Albuquerque

Cedar

Crest

Tijeras

Corrales

Angostura

San

Ysidro

Sandia

Pueblo

San

Felipe

Pueblo

Santo

Domingo

Pueblo

Santo

Ana

Pueblo

Isleta Pueblo

Cochiti

Jemez Pueblo

Pueblo

Zia

Pueblo

Sandoval

Jemez

River

Valencia

Mesita

To ́hajiilee

Rio

Puerco

Inner valley

0 10 20 30 MILES

0 10 20 30 KILOMETERS

Llano de Albuquerque

Manzano Mountains

Sandia Mountains

Ladron

Peak
3

effective stresses to exceed the preconsolidation stress

levels. The magnitude of water-level decline required

to exceed these levels can be estimated using simple

assumptions (Terzaghi, 1925). By assuming similar

depths to the paleowater and modern water tables, an

average grain density of 2.7 grams/cm3

, and porosity of

0.3, the equivalent water-level decline is approximately

1.2 times the thickness of the missing overburden, or

about 120 m. By 1996, ground-water levels had

declined as much as 50 m from steady-state conditions

in some areas of Albuquerque (Bartolino and Cole,

2002).

Purpose and Scope

This report presents the results of a study to

determine potential land-surface displacement in and

near Albuquerque, New Mexico. Interferometric

synthetic aperture radar (InSAR) data were obtained to

help detect small-scale deformation of the aquifer

system resulting from water-level variations. Five

interferograms are presented for selected time intervals

from July 1993 to September 1999.

Methods

InSAR was used to obtain spatially detailed

maps of ground-surface displacements for purposes of

detecting small-scale deformation of the aquifer

system in the upper Albuquerque Basin. This technique

has been successfully applied to investigations of

crustal deformation caused by earthquakes (Massonnet

and others, 1993; Peltzer and others, 1999), volcanoes

(Massonnet and others, 1995; Wicks and others, 1998),

and land subsidence related to the withdrawal of

subsurface fluids for geothermal energy (Massonnet

and others, 1997), oil and gas production (Fielding and

others, 1998), and ground-water resources (Galloway

and others, 1998, 2000; Amelung and others, 1999;

Hoffman and others, 2001).

Acknowledgments

This study was partially funded through a

cooperative agreement between the U.S. Geological

Survey (USGS) and the City of Albuquerque. Radar

data for this study were obtained from the European

Space Agency, distributed through Eurimage

Corporation for purposes of research and development.

RADAR INTERFEROMETRY

Five interferograms were processed using SAR

data (Track 98, Frame 2907) acquired by the European

Remote Sensing (ERS) satellites, ERS-1 and ERS-2,

operated by the European Space Agency. Six SAR

scenes with similar acquisition geometries (absolute

value of the orbital perpendicular baselines less than

150 m) were paired to form five interferograms

covering the period July 2, 1993, to September 13,

1999 (table 1). Interferometric processing was done on

a subarea of the full SAR frame to focus on the

Albuquerque area (fig. 1). To eliminate some of the

noise in the interferograms, the SAR images were

averaged, resulting in a 40-m resolution in both

azimuth (along track) and range (across track)

directions.

Table 1. Selected synthetic aperture radar (SAR) data

acquisitions and interferometric pairs

[--, no data]

1European Remote Sensing (ERS) satellites operated by the European

Space Agency.

The phase component of the complex-valued

interferogram contains information not only about

coherent displacements of reflectors imaged by the

radar, but also topography and propagation delays due

to spatially and temporally variable tropospheric water

SAR data Interferometric pairs

Satellite1

Image

date

Orbit

number

Orbital

pair

Orbital

perpendicular

baseline,

in meters

Time

span,

in

days

ERS-1 7/2/1993 10263 10263-

21629

45 793

ERS-1 9/3/1995 21629 21629-

4962

-39 211

ERS-2 4/1/1996 4962 10263-

4962

6 1,004

ERS-2 2/10/1997 9471 9471-

14982

147 385

ERS-2 3/2/1998 14982 14982-

22998

33 560

ERS-2 9/13/1999 22998 -- -- --
4

content. The effects of topography were removed by

simulating a topographic interferogram in the

geometry of the SAR scenes using a 30-m digital

elevation model (DEM) of the study area and

subtracting it from each. The effect of variable

tropospheric delays was minimized by selecting SAR

scenes acquired during periods of dry weather based on

local meteorological data. To calculate the

interferograms, we used the PRISME/DIAPASON

software (Centre National d’Etudes Spatiales, 1997) in

the two-pass approach described by Massonnet and

others (1994) and Massonnet and Feigl (1998).

The coherent phase component of the resulting

interferograms represents range (line-of-sight)

displacements, mapped modulo 2 Pi (or 28 mm, onehalf the wavelength of the C-band radar). Prior to

unwrapping, the interferogram values were smoothed

using a spectral smoothing algorithm (Z. Lu, U.S.

Geological Survey, written commun., 2000). The

smoothed interferograms were unwrapped using

Escher, an algorithm (Shindle, 1999) that employs the

branch-cut method (Goldstein and others, 1988). The

resulting interferograms were transformed from the

geometry of the radar to cartographic coordinates

(Lambert central meridian = -106 degrees), resampled

at 30-m resolution on the registered grid of the DEM.

By assuming that all the observed range

displacement was due to vertical ground

displacements, the vertical component of the

displacement field was computed from the range

displacements using the 23-degree radar incident angle

(Hanssen, 2001). Interferogram values were verified in

areas of known bedrock outcrop or insignificant

alluvial thickness near the west flank of the Sandia

Mountains (fig. 2), which were presumed to be stable

over the period spanned by the interferogram. Values in

the 793-day interferogram (fig. 2A) were decreased by

5.575 mm to indicate zero displacement over bedrock.

The interferograms are shown in color draped over a

gray-scale shaded-relief image of the area in figure

2A-2E. (Areas in which the interferogram could not be

unwrapped are transparent in these figures, thereby

providing geographic reference from the underlying

shaded relief image.) The interferogram values were

smoothed with a 5 x 5 pixel-averaging filter prior to

generating the displacement profiles (fig. 2).

GROUND-DISPLACEMENT

OBSERVATIONS

793-Day Interferogram (July 2, 1993 -

September 3, 1995)

Rio Rancho

Maximum subsidence of about 48 mm occurs in

Rio Rancho near 35o17’N., 106o

42’W. The area that

has subsided more than 7.6 mm (magenta in fig. 2A)

covers about 12 km2. Rectilinear boundaries on the

northeast and western margins and more diffuse, less

well defined boundaries on the southern and

southeastern margins delimit the subsided area. The

linear west and northeast boundaries roughly parallel

the strikes of mapped faults, shown in figure 2B, about

1 km distant from each boundary. The gradient of

displacement along profile A-A’ (fig. 3) at these

boundaries is relatively large, nearly 1.0 x 10-5 on the

northeast and possibly larger on the west, where signal

decorrelation prevented unwrapping of the

interferogram and gradient calculation.

Albuquerque

Subsidence of 10 to 15 mm in the Albuquerque

region extends from about 5 km west of the Rio Grande

to longitude 106o

30’W. near the Sandia Mountains at

the eastern margin of the interferogram (fig. 2A), and

from latitude 35o

17’N. on the north to 35o3’N. on the

south. Patterns of displacement are distinctive in the

subsided area. An extended line along the strike of the

northeastern boundary of the Rio Rancho subsidence

bowl coincides with a northeastern subsidence

boundary in Albuquerque. Two to three northeasterntrending elongate subsidence lobes with relative

displacement of about 6 mm create an undulating

displacement surface across the region; the troughs of

two prominent undulations are evident in profile B-B’

(fig. 4). Alternatively, these apparent northeasttrending subsidence lobes could be tropospheric

artifacts; signal delays in the September 3, 1995, SAR

data would appear as subsidence in this interferogram.

East of the Rio Grande, near latitude 35o

9’N.,

longitude 106o39’W., a localized, circular-shaped

signal has relative subsidence of about 15 mm. An

elliptical-shaped feature at latitude 35o15’N., longitude

106o

31’W. has a maximum subsidence of 13 mm.
Figure 2A. Interferogram (793 day) showing ground displacement from July 2, 1993, to September 3, 1995.

RIO RANCHO

ALBUQUERQUE

35°

20 ́

35°

15 ́

35°

10 ́

35°

00 ́

35°

05 ́

34°

55 ́

106°55 ́ 106°50 ́ 106°45 ́ 106°40 ́ 106°35 ́ 106°30 ́

0 10 15 20

0 5 10 15 20 25 MILES

5 25 KILOMETERS

RIO

GRANDE

A A ́

B B ́ SANDIA MOUNTAINS

Well producing less than 1,000 acre-feet per year from January to August 1995

Well producing greater than 1,000 acre-feet per year from January to August 1995

EXPLANATION

Uplift Subsidence

Change in land-surface elevation, in millimeters

A-A ́, B-B ́ Trace of profiles shown in figure 3

68 29 10 7 4 2 0 -1.8 -3.5 -5.1 -7.5 -68

TijerasArroyo

U.S. Geological Survey

digital elevation data

5
6

Figure 2B. Interferogram (211 day) showing ground displacement in relation to mapped faults from

September 3, 1995, to April 1, 1996.

35 ̊

20 ́

35 ̊

15 ́

35 ̊

10 ́

35 ̊

00 ́

35 ̊

05 ́

34 ̊

55 ́

106 ̊55 ́ 106 ̊50 ́ 106 ̊45 ́ 106 ̊40 ́ 106 ̊35 ́ 106 ̊30 ́

A A ́

B B ́

EXPLANATION

A-A ́, B-B ́ Trace of profiles shown in figure 3

Change in land-surface elevation, in millimeters

Uplift Subsidence

68 29 10 7 4 2 0 -1.8 -3.5 -5.1 -7.5 -68

Sandia Fault

Fault

Rincon

Coronado

Fault

Eubank

Fault

Alameda Fault

U.S. Geological Survey

digital elevation data

Geology by Kelly, 1977; Hudson and others, 1999; and Connell, 2000

0 10 15 20

0 5 10 15 20 25 MILES

5 25 KILOMETERS
7

35 ̊

20 ́

35 ̊

15 ́

35 ̊

10 ́

35 ̊

00 ́

35 ̊

05 ́

34 ̊

55 ́

106 ̊55 ́ 106 ̊50 ́ 106 ̊45 ́ 106 ̊40 ́ 106 ̊35 ́ 106 ̊30 ́

Figure 2C. Interferogram (1,004 day) showing ground displacement from July 2, 1993, to April 1, 1996.

Southern Blvd

Unser Blvd

Sandia Indian

Reservation

Sandia

National

Laboratories

Rio Rancho Blvd

Northern Blvd

A A ́

B B ́

EXPLANATION

A-A ́, B-B ́ Trace of profiles shown in figure 3

Change in land-surface elevation, in millimeters

Uplift Subsidence

68 29 10 7 4 2 0 -1.8 -3.5 -5.1 -7.5 -68

U.S. Geological Survey

digital elevation data

Tramway Blvd

0 10 15 20

0 5 10 15 20 25 MILES

5 25 KILOMETERS
8

35 ̊

20 ́

35 ̊

15 ́

35 ̊

10 ́

35 ̊

00 ́

35 ̊

05 ́

34 ̊

55 ́

106 ̊55 ́ 106 ̊50 ́ 106 ̊45 ́ 106 ̊40 ́ 106 ̊35 ́ 106 ̊30 ́

RIO

GRANDE

A A ́

B B ́

EXPLANATION

Uplift Subsidence

68 29 10 7 4 2 0 -1.8 -3.5 -5.1 -7.5 -68

Tijeras Arroyo

BOREHOLE

EXTENSOMETER

GARFIELD

DEL SOL DIVIDER

SISTER CITIES

Piezometer site

A-A ́, B-B ́ Trace of profiles shown in figure 3

Change in land-surface elevation, in millimeters

U.S. Geological Survey

digital elevation data

0 10 15 20

0 5 10 15 20 25 MILES

5 25 KILOMETERS

Figure 2D. Interferogram (385 day) showing ground displacement from February 10, 1997, to March 2, 1998.
9

0 10 15 20

0 5 10 15 20 25 MILES

5 25 KILOMETERS

Figure 2E. Interferogram (560 day) showing ground displacement from March 2, 1998, to September 13, 1999.

35 ̊

20 ́

35 ̊

15 ́

35 ̊

10 ́

35 ̊

00 ́

35 ̊

05 ́

34 ̊

55 ́

106 ̊55 ́ 106 ̊50 ́ 106 ̊45 ́ 106 ̊40 ́ 106 ̊35 ́ 106 ̊30 ́

A A ́

B B ́

EXPLANATION

A-A ́, B-B ́ Trace of profiles shown in figure 3

Change in land-surface elevation, in millimeters

Uplift Subsidence

68 29 10 7 4 2 0 -1.8 -3.5 -5.1 -7.5 -68

Tijeras

Arroyo

RIO GRANDE

U.S. Geological Survey

digital elevation data

GARFIELD

DEL SOL DIVIDER

EXTENSOMETER

SISTER CITIES
10

A: Profile A-A': July 2, 1993 - September 3, 1995

B: Profile A-A': September 3, 1995 - April 1, 1996

E: Profile A-A': March 2, 1998 - September 13, 1999

Distance along profile, in kilometers

D: Profile A-A': February 10, 1997 - March 2, 1998

C: Profile A-A': July 2, 1993 - April 1, 1996

-45

-35

-25

-15

-5

5

15

25

35

-45

-35

-25

-15

-5

5

15

25

35

-45

-35

-25

-15

-5

5

15

25

35

-45

-35

-25

-15

-5

5

15

25

35

-45

-35

-25

-15

-5

5

15

25

35

D i s p l a c e m e n t , i n m i l l i m e t e r s

0 10 20 30 40

Figure 3. Vertical displacement along profile A-A ́ from July 2, 1993, to September 13, 1999.

Trace of profile in figure 2A-2E.
11

A: Profile B-B': July 2,1993 - September 3, 1995

-45

-35

-25

-15

-5

5

15

25

35

B: Profile B-B': September 3, 1995 - April 1, 1996

-45

-35

-25

-15

-5

5

15

25

35

D: Profile B-B': February 10, 1997 - March 2, 1998

-45

-35

-25

-15

-5

5

15

25

35

C: Profile B-B': July 2, 1996 - April 1, 1996

-45

-35

-25

-15

-5

5

15

25

35

E: Profile B-B': March 2, 1998 - September 13, 1999

Distance along profile, in kilometers

-45

-35

-25

-15

-5

5

15

25

35

0 10 20 30 40

D i s p l a c e m e n t , i n m i l l i m e t e r s

Figure 4. Vertical displacement along profile B-B ́ from July 2, 1993, to September 13, 1999.

Trace of profile in figure 2A-2E.
12

211-Day Interferogram (September 3, 1995

- April 1, 1996)

Rio Rancho

An uplift of magnitude 24 mm (fig. 2B) is

observed in the location of the prominent subsidence

zone on the 793-day interferogram (fig. 2A). The

gradient of displacement measured along profile A-A’

(fig. 3) across the western and northeastern boundaries

is -2.6 x 10-5 and -7.8 x 10-6, respectively. The good

coherence of this image reveals a linear boundary along

the eastern portion of the uplift feature (yellow fringe

along profile A-A’ in fig. 2B), which is subparallel to

the western boundary of the uplift feature. This uplift

zone has a quadrilateral shape, similar to the spatially

coincident subsidence zone on the 793-day

interferogram.

An elongate subsidence feature near longitude

106o43’W. (blue and magenta-purple pattern in fig. 2B)

extends south to latitude 35o

10’N. The eastern

boundary of this prominent south-trending lobe

conforms to the mapped location of south-trending

faults (fig. 2B). The gradients of displacement from the

lobe margins to the location of maximum subsidence

are smaller (1.9 x 10-6 and 3.9 x 10-6, respectively; fig.

3) than those of the rectilinear feature described earlier.

The southern portion of this lobe also appears as

subsidence in the 793- and 1,004-day interferograms

(fig. 2A,2C). To the west, a south-trending zone (green)

indicates uplift of about 5 mm (fig. 2B). This area could

not be unwrapped in the 793-day or 1,004-day

interferograms.

Albuquerque

The undulating displacement surface observed in

Albuquerque in the 793-day interferogram (fig. 2A)

appears with reverse sense: subsidence troughs have

become uplift ridges (fig. 2B). The apparent northeasttrending uplift ridges corresponding to the subsidence

lobes observed in figure 2A could be tropospheric

artifacts: signal delays in the September 3, 1995, SAR

data would appear as uplift in this interferogram. The

elliptical-shaped feature at latitude 35o

15’N., longitude

106o31’W. observed in the 793-day interferogram now

appears as 13 mm of uplift. Some subsidence is

observed at latitude 35o17’N., longitude 106o39’W.

The gradient of displacement along profile B-B’ is

presented in figure 4.

1,004-Day Interferogram (July 2, 1993 -

April 1, 1996)

Rio Rancho

Prominent features in this interferogram are

similar locations to those described for the 793-day

interferogram. A maximum of 21 mm of subsidence

occurs near the center of the quadrilateral-shaped

feature in figures 2C and 3. To the southwest, a broad

feature with as much as 14 mm of subsidence extends

nearly 5 km east to west. Displacement gradients on the

margins of this feature average 2.0 x 10-6 (fig. 2C).

Albuquerque

The undulating displacement surface and other

features observed in the 793- and 211-day

interferograms are not obvious in figures 2C and 4.

West of Tramway Boulevard, near latitude 35o9’N.,

longitude 106o33’W., a localized signal with 8 mm of

subsidence is evident. Subsidence west of the Rio

Grande near latitude 35o

9’N., longitude 106oW. is

about 10-15 mm.

385-Day Interferogram (February 10, 1997

- March 2, 1998)

Rio Rancho

The quadrilateral-shaped feature previously

discussed (fig. 2B) is discernible with small magnitude

uplift (yellow) in figures 2D and 3. Minor subsidence is

observed at latitude 35o16’N., longitude 106o39’W.

The sense of deformation for each of these features is

opposite that observed in the 793- and 1,004-day

interferograms.

Albuquerque

Little net displacement occurred in the

Albuquerque area during this nearly 1-year period.

560-Day Interferogram (March 2, 1998 -

September 13, 1999)

Atmospheric artifacts that were evident in the

southwestern and northwestern corners of this

interferogram were removed and appear transparent in

figure 2E. The area shaded red along the east side is

topographically related and may be due to decreasing

density of uplifted air. Good coherence was obtained

over most of the Albuquerque and Rio Rancho areas.
13

Rio Rancho

Subsidence features observed in the previous

four interferograms (fig. 2A-2D) are presented in

figures 2E and 3, albeit with smaller magnitudes.

Albuquerque

Minor displacement (less than 5 mm) is observed

over most of Albuquerque. An uplift feature trending

west-northwest near Tijeras Arroyo and a localized

subsidence area just east of the Rio Grande at latitude

35o

4’N. (purple) are possible exceptions.

Other Measurements

A borehole extensometer east of the Rio Grande

(fig. 2D) in Albuquerque (Heywood, 1997, 1998)

measures compaction in the interval 5-315 m below

land surface. At the extensometer site, completed in

December 1994, a continuous-analog compaction time

series and discrete 15-minute digital compaction and

associated piezometric time series are recorded. The

displacement time history at the extensometer shows 1-

mm-level daily and seasonal variations in response to

water-level variations at a nearby production well. For

the time corresponding to the 211-day interferogram

(fig. 2B), accounting for the 1748-hour Greenwich

Mean Time (GMT) orbital pass-over, 1.7 mm of uplift

was measured on the extensometer. The

interferometrically derived displacement in the pixel

containing the extensometer is 2.1 mm of uplift;

averaging of 2 x 2 pixels and 4 x 4 pixels centered on

the extensometer site gives 1.3 and 1.4 mm of uplift,

respectively. The other interferograms were similarly

compared to the extensometric data.

The USGS and City of Albuquerque installed a

geodetic land-subsidence monitoring network in 1993,

which was surveyed with the GPS in 1993 and 1994.

For 1993-94, the maximum computed benchmark

elevation change of -2 cm was observed near a well in

Rio Rancho. Other computed benchmark elevation

changes were less than 2 cm, which was considered the

limit of resolution of the differential GPS survey. The

time span between the GPS surveys is less than, and

contained within, the period of the first (793-day)

interferogram. The negligible vertical displacements

measured at discrete benchmarks using GPS over

1993-94 agree with those in the 793-day interferogram.

Correlation with Ground-Water-Level

Changes

Ground-water levels in the Albuquerque area

exhibit annual periodicity superimposed on a longterm decline. Hydrographs of selected piezometers

(fig. 5A,5B) reveal that deep ground-water levels (that

is, in wells screened more than 100 m below the water

table) recover during the autumn and early winter

months and typically attain their maximum levels in

January and February. Deep ground-water levels

decline during spring and early summer months and

typically reach minimum levels in July and August.

Seasonal variations in municipal ground-water

pumping contribute to this cyclic response. Landsurface elevation changes observed in the

interferograms (fig. 2A-2E) follow these trends in deep

ground-water-level changes. This spatial and temporal

correspondence suggests that observed apparent landsurface elevation changes result from elastic

compression and expansion of the aquifer-system

skeletal matrix resulting from pore-fluid-pressure

changes.

At the Garfield piezometer site (figs. 2D, 5A) in

the Rio Grande Valley, seasonal variations of the water

table and deeper water levels are out of phase. The

higher water table increases the geostatic load and

hence the effective stress and consequent aquifersystem skeletal matrix compression in the deeper zones

hydraulically separated from the water table. Relative

to in-phase variations, this out-of-phase relation

between the water table and deeper water levels should

accentuate the aquifer-system compression resulting

from a given magnitude of water-level change.

The 793-day interferogram (July 2, 1993, to

September 3, 1995; fig. 2A) corresponds to a period

during which net annual ground-water levels declined

relatively rapidly in the Albuquerque and Rio Rancho

areas. Few water-level observation piezometers existed

in the area at that time, but water-level records for

Albuquerque production wells indicate that annual

declines were about 1-2 m per year. Two seasonal

periods of water-level recovery are encompassed in this

interferogram, during which ground water flowed

locally toward the loci of previous extractions. The

observed subsidence features are therefore biased

toward ground-water extractions that occurred during

the final period of seasonal water-level declines. To

enhance correlation between ground-water extraction

and subsidence, extractions from ground-water supply

wells were totaled for January through August 1995

and are shown in figure 5A.
14

Figure 5A. Depth to water in Garfield piezometers. Location of piezometer site in figure 2D.

Screen: 13-25 meters (water table)

Screen: 168-174 meters

Screen: 303-308 meters

10

12

14

16

18

20

Jan 97

July 97

Jan 98

July 98

Jan 99

July 99

Jan 00

July 00

Jan 01

July 01

Depth to water, in meters

Figure 5B. Depth to water in Del Sol Divider piezometers. Location of piezometer site in figure 2D.

Screen: 96-126 meters (water table)

Screen: 254-255 meters

Screen: 475-476 meters

100

102

104

106

108

110

Jan 97

July 97

Jan 98

Jan 99

Jan 00

Jan 01

July 98

July 99

July 00

July 01

Depth to water, in meters

No data

No data

No data
15

The subsequent 211-day (September 3, 1995, to

April 1, 1996; fig. 2B) interferogram encompasses a

period of seasonal water-level recovery. The reversed

sense of deformation (that is, uplift in locations of

subsidence features observed in the previous 793-day

interferogram) is the elastic response of the aquifer

system to recovering water levels.

The 1,004-day interferogram (fig. 2C; July 2,

1993, to April 1, 1996) encompasses 2 3/4 years of

long-term water-level decline with an extra seasonal

recovery period superimposed. Although subsidence

and uplift features are observed in this interferogram,

subsidence features predominate. Considering the

summer to late-winter seasonal span by the

interferogram and the widespread uplift observed in the

211-day (fig. 2B) interferogram (presumably during a

period of water-level recovery), it is probable that

permanent (inelastic) compaction and subsidence are

accumulating over yearly or longer time scales. This is

partly corroborated by the subsidence observed in the

793-day interferogram (fig. 2A). Because water-level

data do not exist for these areas during the time

spanned by these interferograms, it is not possible to

determine conclusively whether the subsidence is

recoverable (elastic) or permanent. In Rio Rancho,

profile A-A’ crosses the prominent quadrilateralshaped feature, for which the magnitude of subsidence

observed in the 793-day (fig. 2A) interferogram and

subsequent elastic rebound observed in the 211-day

(fig. 2B) interferogram are about 48 and 24 mm,

respectively.

The 385-day interferogram (fig. 2D; February

10, 1997, to March 2, 1998) closely encompasses one

cyclic period of seasonal water-level change. Minimal

net water-level change was observed in the Garfield

and Del Sol Divider piezometers (fig. 5A,5B) during

this time, and insignificant land-surface elevation

change is observed at these locations in the

interferogram. The water level in the Sister Cities 1

piezometer (site location shown in fig. 2D) declined

1.74 m during this period; subsidence is observed in

this area of north Albuquerque. Displacement features

in Rio Rancho exhibit both subsidence and elastic

rebound, presumably in response to net ground-waterlevel changes.

The 560-day interferogram (fig. 2E; March 2,

1998, to September 13, 1999) again encompasses a

period with both long-term and seasonal water-level

changes superimposed. Hydrographs for deeper

piezometers at the Garfield and Del Sol Divider sites

(fig. 5A,5B) indicate about 2 and 4 m, respectively, of

net water-level decline during this period. Relatively

small and uniform subsidence is observed in this area

of the interferogram.

Geologic Structures in the Study Area that

Influence Ground-Water Flow

The quadrilateral-shaped displacement feature

observed in Rio Rancho in all five interferograms, and

particularly the 211-day interferogram (fig. 2B),

correlates with the location of the Zia Horst, a known

fault-bounded, local structural uplift. This horst

juxtaposes relatively permeable, well-sorted sand of

the Zia Sand of Tertiary age against outlying,

stratigraphically younger sediment. Greater diagenetic

cementation (Sean Connell, New Mexico Bureau of

Geology and Mineral Resources, oral commun., 2001)

in the outlying sediment may have imparted a lower

permeability and compressibility to this sediment;

horst-bounding faults also appear to impede groundwater flow. Subsidence is observed over the Zia Horst

in the 793-day interferogram (fig. 2A), presumably due

to pumpage from a well near the west fault-bounded

side of the structure. The subsequent 211-day

interferogram (fig. 2B) shows elastic rebound over this

structure as ground-water levels recovered. The lightblue subsidence lobes northwest and northeast of this

block of relatively high permeability suggest that water

levels declined in those areas during this 211-day

period, though no significant ground-water

withdrawals occurred. These water-level declines may

be a response to drawdown in this area during the

previous interferogram period, which was delayed by

low permeability of the block-bounding faults. This

interpretation suggests the possibility that the waterlevel response inferred from a continuous series of

short temporal-baseline interferograms could be used

to estimate the effective hydraulic conductivity of a

fault “flow barrier” in an elastically deforming aquifer

system.

On the east side of the interferograms, the

Rincon and Sandia normal faults (fig. 2B) are basinbounding structures that separate crystalline rock of

Precambrian age to the east from basin-fill alluvium of

Tertiary and Quaternary age (Kelly, 1977) to the west;

the eastern limit of the observed InSAR-derived

displacements in Albuquerque corresponds with this

boundary. The Alameda, Eubank, and Coronado Faults

are north-trending, west-dipping normal faults that
16

make up the east heights fault zone. Offsets in deposits

of Tertiary and Quaternary age observed in drill-hole

lithologic and geophysical logs were used to map these

faults. The boundaries of the displacement lobes

observed in the 793- and 211-day interferograms (fig.

2A,2B) correlate well with the mapped extent of these

faults, suggesting that the faults have low permeability,

which impedes the propagation of water-level changes.

As noted in the Ground-displacement observations

section for the 793- and 211-day interferograms, these

apparent subsidence and elastic-rebound lobes could

be artifacts resulting from localized tropospheric

delays in the September 3, 1995, SAR data.

An additional interferogram spanning a time

with similar water-level variations would help

discriminate between these alternatives. The 385-day

(fig. 2D) interferogram does not span a time with

significant seasonal water-level change. The 560-day

(fig. 2E) interferogram spans such a seasonal change

but was contaminated by atmospheric effects in the

area of interest. SAR data from January to August 1997

were collected and span a time with seasonal waterlevel variation. An interferogram processed from these

data may further illuminate the presence of

permeability barriers in the Albuquerque and Rio

Rancho areas.

The north-south trends of the northeast heights

faults (fig. 2B) are from a compilation by Hudson and

others (1999). Connell (2000) interpreted a

northwesterly trend divergence of these faults in north

Albuquerque, in accordance with a regional structural

interpretation (John Hawley, oral commun., 2000). The

northwesterly trend of the eastern boundary of the

subsidence lobe in figure 2A may support this

interpretation. Because water-level change (and

consequent observed elastic compression) is a

convolved response to pumping and spatially variable

aquifer-system hydraulic diffusivities, it is difficult to

discriminate the hydraulic effect of these structural

alternatives without ground-water flow modeling.

Plummer and others (2001) mapped zones of

different water quality in the Albuquerque area.

Differences in stable isotopes discriminate zones

containing ground water recharged from the Sandia

Mountains or the Rio Grande. The boundary between

two zones generally corresponds with the northeast

heights fault zone location, further suggesting that

ground-water flow from the mountain front is impeded

by low-permeability faults, such as the Alameda,

Eubank, and Coronado strands of the northeast heights

fault zone.

CONCLUSIONS

Interferometric measurements of land-surface

elevation change suggest that aquifer-system

compression resulting from ground-water withdrawals

in the Albuquerque area has probably remained elastic

(recoverable) from July 1993 through September 1999.

Evidence suggests that some inelastic (permanent)

compaction and land subsidence may have occurred in

the Rio Rancho area, but this cannot be concluded

because of the absence of ground-water-level data for

the same periods of the interferograms. Patterns of land

subsidence and uplift in both Albuquerque and Rio

Rancho suggest that intrabasin faults may impede

ground-water diffusion at seasonal time scales.

Alternatively, apparent patterns of compression and

elastic rebound may result from spatially coincident

tropospheric delay effects in the September 3, 1995,

SAR data. An additional interferogram spanning the

time from January to August 1997 may help

discriminate between these alternatives.

SELECTED REFERENCES

Amelung, F., Galloway, D.L., Bell, J.W., Zebker, H.A., and

Laczniak, R.J., 1999, Sensing the ups and downs of Las

Vegas—InSAR reveals structural control of land

subsidence and aquifer-system deformation: Geology,

v. 27, p. 483-486.

Bartolino, J.R., and Cole, J.C., 2002, Ground-water

resources of the Middle Rio Grande Basin, New

Mexico: U.S. Geological Survey Circular 1222, 132 p.

Bawden, G.W., Thatcher, W., Stein, R.S., Hudnut, K.W., and

Peltzer, G., 2001, Tectonic contraction across Los

Angeles after removal of groundwater pumping effects:

Nature, v. 412, p. 812-815.

Bell, J.W., 1981a, Results of leveling across fault scarps in

Las Vegas Valley, Nevada, April 1978 - June 1981:

Nevada Bureau of Mines and Geology Open-File

Report 81-5, 7 p.

———1981b, Subsidence in Las Vegas Valley: Nevada

Bureau of Mines and Geology Bulletin 95, 83 p., 1 pl.

Bell, J.W., and Price, J.G., 1993, Subsidence in Las Vegas

Valley, 1980-91—Final project report: Nevada Bureau

of Mines and Geology Open-File Report 93-4, 10

sections, 9 pls., variously paged.

Carpenter, M.C., 1993, Earth-fissure movements associated

with fluctuations in ground-water levels near the
17

Picacho Mountains, south-central Arizona, 1980–84:

U.S. Geological Survey Professional Paper 497-H,

49 p.

Carpenter, M.C., 1999, South-central Arizona—Earth

fissures and subsidence complicate development of

desert water resources, in Galloway, D.L., Jones, D.R.,

and Ingebritson, S.E., eds., Land subsidence in the

United States: U.S. Geological Survey Circular 1182,

p. 65-78.

Centre National d'Etudes Spatiales (C.N.E.S.), 1997,

PRISME/DIAPASON Software: Toulouse, France,

version 1.0.

Connell, S.D., 2000, Geology of the Alameda quadrangle,

Bernalillo and Sandoval Counties, New Mexico:

Socorro, New Mexico Bureau of Mines and Mineral

Resources Open-File Map GM-10, 1 sheet, scale

1:24,000.

Fielding, E.J., Blom, R.G., and Goldstein, R.M., 1998, Rapid

subsidence over oil fields measured by SAR

interferometry: Geophysical Research Letters, v. 27,

p. 3,215-3,218.

Gabriel, A.K., Goldstein, R.M., and Zebker, H.A., 1989,

Mapping small elevation changes over large

areas—Differential radar interferometry: Journal of

Geophysical Research, v. 94, p. 9,183-9,191.

Galloway, D.L., Hudnut, K.W., Ingebritsen, S.E., Phillips,

S.P., Peltzer, G., Rogez, F., and Rosen, P.A., 1998,

Detection of aquifer system compaction and land

subsidence using interferometric synthetic aperture

radar, Antelope Valley, Mojave Desert, California:

Water Resources Research, v. 34, p. 2,573-2,585.

Galloway, D.L., Jones, D.R., and Ingebritsen, S.E., eds.,

1999, Land subsidence in the United States: U.S.

Geological Survey Circular 1182, 175 p.

———2000, Measuring land subsidence from space: U.S.

Geological Survey Fact Sheet 051-00, 4 p.

Goldstein, R.M., Zebker, H.A., and Werner, C.L., 1988,

Satellite radar interferometry—Two-dimensional phase

unwrapping: Radio Science, v. 23, no. 4, p. 713-720.

Hanssen, R.F., 2001, Radar interferometry: Boston, Kluwer

Academic Publishers, 308 p.

Heywood, C.E., 1997, Piezometric-extensometric

estimations of specific storage in the Albuquerque

Basin, New Mexico, in Prince, K.R., and Leake, S.A.,

eds., U.S. Geological Survey Subsidence Interest

Group Conference--Proceedings of the technical

meeting, Las Vegas, Nevada, February 14-16, 1995:

U.S. Geological Survey Open-File Report 97-47, p.

21-26.

———1998, Piezometric-extensometric estimations of

specific storage in the Albuquerque Basin, New

Mexico, in Borchers, J.W., ed., Land subsidence case

studies and current research: Proceedings of the Dr.

Joseph F. Poland Symposium on Land Subsidence,

Association of Engineering Geologists Special

Publication no. 8, p. 435-440.

Hoffmann, Jörn, Zebker, H.A., Galloway, D.L., and

Amelung, F., 2001, Seasonal subsidence and rebound in

Las Vegas Valley, Nevada, observed by synthetic

aperture radar interferometry: Water Resources

Research, v. 37, no. 6, p. 1,551-1,566.

Holzer, T.L., 1998, History of the aquitard-drainage model in

land subsidence case studies and current research, in

Borchers, J.W., ed., Land subsidence case studies and

current research: Proceedings of the Dr. Joseph F.

Poland Symposium on Land Subsidence, Association

of Engineering Geologists Special Publication no. 8,

p. 7–12.

Hudson, M.R., Minor, S.A., Grauch, V.J.S., and Personius,

S.F., 1999, Preliminary characterization of faults in the

Middle Rio Grande Basin, in Bartolino, J.R., ed., U.S.

Geological Survey Middle Rio Grande Basin

Study—Proceedings of the Third Annual Workshop,

Albuquerque, New Mexico, February 24-25, 1999: U.S.

Geological Survey Open-File Report 99-203, p. 40-41.

Ikehara, M.E., Galloway, D.L., Fielding, E.J., Bürgmann, R.,

Lewis, A.S., and Ahmadi, B., 1998, InSAR imagery

reveals seasonal and longer-term land-surface elevation

changes influenced by ground-water levels and fault

alignment in Santa Clara Valley, California [abs.]: EOS

(supplement) Transactions, American Geophysical

Union, no. 45, November 10, 1998, p. F37.

Ikehara, M.E., and Phillips, S.P., 1994, Determination of

land subsidence related to ground-water-level declines

using global positioning system and leveling surveys in

Antelope Valley, Los Angeles and Kern Counties,

California, 1992: U.S. Geological Survey WaterResources Investigations Report 94-4184, 101 p.

Ireland, R.L., Poland, J.F., and Riley, F.S., 1984, Land

subsidence in the San Joaquin Valley, California, as of

1980: U.S. Geological Survey Professional Paper 437-

I, 93 p.

Kelly, V.C., 1977, Geology of the Albuquerque basin, New

Mexico: Socorro, New Mexico Bureau of Mines and

Mineral Resources Memoir 33, 60 p.

Laney, R.L., Raymond, R.H., and Winikka, C.C., 1978,

Maps showing water-level declines, land subsidence,

and earth fissures in south-central Arizona: U.S.

Geological Survey Water-Resources Investigations

Report 78-83, 2 sheets, scale 1:125,000.

Machette, M.N., Personius, S.F., Kelson, K.I., Haller, K.M.,

and Dart, R.L., 1998, Map and data for Quaternary

faults in New Mexico: U.S. Geological Survey OpenFile Report 98-521, 443 p., 1 pl., scale 1:750,000.

Massonnet, D., Briole, P., and Arnaud, A., 1995, Deflation of

Mount Etna monitored by spaceborne radar

interferometry: Nature, v. 375, p. 567-570.
18

Massonnet, D., and Feigl, K.L., 1998, Radar interferometry

and its application to changes in the Earth's surface:

Reviews of Geophysics, v. 36, p. 441-500.

Massonnet, D., Feigl, K.L., Rossi, M., and Adragna, F.,

1994, Radar interferometric mapping of deformation in

the year after the Landers earthquake: Nature, v. 369,

p. 227-230.

Massonnet, D., Holzer, T.L., and Vadon, H., 1997, Land

subsidence caused by the East Mesa geothermal field,

California, observed using SAR interferometry:

Geophysical Research Letters, v. 24, p. 901-904.

Massonnet, D., Rossi, M., Carmona, C., Adragna, F., Peltzer,

G., Feigl, K.L., and Rabaute, T., 1993, The

displacement field of the Landers earthquake mapped

by radar interferometry: Nature, v. 364, p. 138-142.

Moore, S.J., and Anderholm, S.K., 2001, Ground-water

monitoring in the Middle Rio Grande Basin, central

New Mexico—Implications of water-level variations in

nested piezometers [abs.]: Geological Society of

America, 2001 Abstracts with Programs, Rocky

Mountain and South-Central Sections, v. 33, no. 5,

p. A-54.

National Research Council, 1991, Mitigating losses from

land subsidence in the United States: Washington, D.C.,

National Academy Press, 58 p.

Peltzer, G., Crampe, F., and King, G., 1999, The Mw7.6,

Manyi (Tibet) earthquake—Surface rupture, surface

displacement field, and fault slip solution from ERS

SAR data: EOS, Transactions of the American

Geophysical Union, v. 80, no. 46, p. 1,023.

Plummer, L.N., Bexfield, L.M., Anderholm, S.K., Sanford,

W.E., and Busenberg, Eurybiades, 2001, Geochemical

characterization of ground-water flow in parts of the

Santa Fe Group aquifer system, Middle Rio Grande

Basin, New Mexico, in Cole, J.C., ed., U.S. Geological

Survey Middle Rio Grande Basin Study—Proceedings

of the Fourth Annual Workshop, Albuquerque, New

Mexico, February 15-16, 2000: U.S. Geological Survey

Open-File Report 00-488, p. 7-10.

Poland, J.F., ed., 1984, Guidebook to studies of land

subsidence due to ground-water withdrawal: Paris,

United Nations Educational, Scientific and Cultural

Organization, Studies and reports in hydrology 40,

305 p.

Poland, J.F., and Ireland, R.L., 1988, Land subsidence in the

Santa Clara Valley, California, as of 1982: U.S.

Geological Survey Professional Paper 497-F, 61 p.

Poland, J.F., Lofgren, B.E., Ireland, R.L., and Pugh, R.G.,

1975, Land subsidence in the San Joaquin Valley,

California, as of 1972: U.S. Geological Survey

Professional Paper 437-H, 78 p.

Rosen, P.A., Hensley, S., Zebker, H.A., Webb, F.H., and

Fielding, E.J., 1996, Surface deformation and

coherence measurements of Kilauea volcano, Hawaii,

from SIR-C radar interferometry: Journal of

Geophysical Research, v. 101, p. 23, 109-23, 125.

Shindle, M., 1999, ESCHER—An algorithm for unwrapping

an interferogram phase file using the branch-cut

method: Fairbanks, Alaska SAR Facility.

Sneed, Michelle, and Galloway, D.L., 2000, Aquifer-system

compaction and land subsidence—Measurements,

analyses, and simulations—the Holly site, Edwards Air

Force Base, Antelope Valley, California: U.S.

Geological Survey Water-Resources Investigations

Report 00-4015, 65 p.

Sneed, Michelle, Ikehara, M.E., Galloway, D.L., and

Amelung, F., 2001, Detection and measurement of land

subsidence using global positioning system and

interferometric synthetic aperture radar, Coachella

Valley, California: U.S. Geological Survey WaterResources Investigations Report 01-4193, 26 p.

Terzaghi, Karl, 1925, Erdbaumechanik auf

Bodenphysikalischer Grundlage: Wein Leipzig,

Deuticke, 399 p.

Vadon, H., and Sigmundsson, F., 1997, 1992-1995 crustal

deformation at Mid-Atlantic ridge, SW Iceland,

mapped by radar interferometry: Science, v. 275,

p. 193-197.

Wicks, C., Jr., Thatcher, W., and Dzurisin, D., 1998,

Migration of fluids beneath Yellowstone Caldera

inferred from satellite radar interferometry: Science,

v. 282, p. 458-462.

Zebker, H.A., Rosen, P.A., Goldstein, R.M., Gabriel, A.K.,

and Werner, C.L., 1994, On the derivation of coseismic

displacement fields, using differential radar

interferometry—The Landers earthquake: Journal of

Geophysical Research, v. 99, p. 19,617-19,634.
C.E. Heywood, D.L. Galloway, and S.V. Stork—GROUND DISPLACEMENTS CAUSED BY AQUIFER-SYSTEM WATER-LEVEL VARIATIONS

OBSERVED USING INTERFEROMETRIC SYNTHETIC APERTURE RADAR NEAR ALBUQUERQUE, NEW MEXICO—U.S. Geological Survey

Water-Resources Investigations Report 02-4235

U.S. Department of the Interior

U.S. Geological Survey, WRD

5338 Montgomery Blvd. NE, Suite 400

Albuquerque, NM 87109-1311

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