Prepared in cooperation with the Scott Polar Research Institute, 

University of Cambridge, United Kingdom

Coastal-Change and Glaciological Map of the 

Ross Island Area, Antarctica: 1962–2005

By Jane G. Ferrigno, Kevin M. Foley, Charles Swithinbank, 

and Richard S. Williams, Jr.

Pamphlet to accompany

Geologic Investigations Series Map I–2600–I

2010

U.S. Department of the Interior

U.S. Geological Survey
U.S. Department of the Interior

KEN SALAZAR, Secretary

U.S. Geological Survey

Marcia K. McNutt, Director

U.S. Geological Survey, Reston, Virginia: 2010

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reproduce any copyrighted materials contained within this report.

Suggested citation:

Ferrigno, J.G., Foley, K.M., Swithinbank, Charles, and Williams, R.S., Jr., 2010, Coastal-change and glaciological map 

of the Ross Island area, Antarctica: 1962–2005: U.S. Geological Survey Geologic Investigations Series Map I–2600–I, 

1 map sheet, 23-p. text.

ISBN 978-1-4113-2477-0
iii

Contents

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

Background ...........................................................................................................................................1

Objectives...............................................................................................................................................2

Sources...................................................................................................................................................3

Methodology ..........................................................................................................................................3

RADARSAT Image Mosaic of Antarctica and its Geodetic Accuracy .........................................4

Geographic Description ................................................................................................................................4

Glacier Inventory and Glaciological Features ..........................................................................................4

Coastal-Change Analysis—Discussion of Selected Glaciological Features ......................................5

Glaciers that Drain from or through the Transantarctic Mountains .............................................5

Byrd Glacier ..................................................................................................................................5

Darwin Glacier..............................................................................................................................6

Hatherton Glacier ........................................................................................................................6

Mulock Glacier .............................................................................................................................6

Skelton Glacier .............................................................................................................................6

Koettlitz Glacier ............................................................................................................................6

Erebus Glacier Tongue .........................................................................................................................6

McMurdo Dry Valleys ..........................................................................................................................7

Icebergs..................................................................................................................................................7

Ice Cores ................................................................................................................................................7

Blue-Ice Areas and Meteorites ..........................................................................................................8

Subglacial Lakes ...................................................................................................................................8

Summary..........................................................................................................................................................9

Acknowledgments .........................................................................................................................................9

References Cited............................................................................................................................................9

Appendix—Tables 2 and 3 ..........................................................................................................................15

Figures

 1. Index map of the planned and published 1:1,000,000-scale coastal-change and glaciological maps of Antarctica ..........................................................................................................2

 2. Location map of Antarctica showing West and East Antarctica, the Transantarctic 

Mountains, the Ross Ice Shelf, and the Antarctic Peninsula ................................................4
iv

Tables

 1. Coastal-change and glaciological maps of Antarctica at 1:1,000,000 scale, published to 

date .................................................................................................................................................2

 2. Topographic, satellite image, and photo maps in the Ross Island map area, produced 

by the USGS and cooperators ..................................................................................................16

 3. Inventory of named glaciers and glaciological features on the coastal-change and 

glaciological map of the Ross Island area .............................................................................19

Conversion Factors

Multiply By To obtain

meter (m)

kilometer (km)

Length

3.281

0.6214

foot (ft) 

mile (mi)

Area

square kilometer (km2

) 0.3861 square mile (mi2)

Volume

cubic kilometer (km3

) 0.2399 cubic mile (mi3) 
Coastal-Change and Glaciological Map of the 

Ross Island Area, Antarctica: 1962–2005

By Jane G. Ferrigno,1 Kevin M. Foley,1 Charles Swithinbank,2 and Richard S. Williams, Jr.3

Introduction

Background 

Reduction in the area and volume of the two polar ice 

sheets is intricately linked to changes in global climate, 

and the resulting rise in sea level could severely impact the 

densely populated coastal regions on Earth. Antarctica is 

Earth’s largest reservoir of glacial ice. Melting of the West 

Antarctic part alone of the Antarctic ice sheet would cause a 

sea-level rise of approximately 6 meters (m), and the potential 

sea-level rise after melting of the entire Antarctic ice sheet 

is estimated to be 65 m (Lythe and others, 2001) to 73 m 

(Williams and Hall, 1993). Shepherd and Wingham (2007) 

discussed change in the Antarctic ice sheet as part of the 

global picture, and Jenkins and Holland (2007) discussed the 

real potential of sea-level rise from the melting of floating ice 

such as ice shelves and icebergs. The mass balance (the net 

volumetric gain or loss) of the Antarctic ice sheet is highly 

complex, responding differently to different climatic and other 

conditions in each region (Vaughan, 2005). In a review paper, 

Rignot and Thomas (2002) concluded that the West Antarctic 

ice sheet is probably becoming thinner overall; although it 

is known to be thickening in the west, it is thinning in the 

north. Thomas and others (2004), on the basis of aircraft and 

satellite laser altimetry surveys, believe that the thinning may 

be accelerating. Joughin and Tulaczyk (2002), on the basis of 

ice-flow velocities derived from analysis of synthetic-aperture 

radar data, concluded that most of the Ross ice streams (ice 

streams flowing into the east side of the Ross Ice Shelf) have a 

positive mass balance, whereas Rignot and others (2004) infer 

a larger negative mass balance for glaciers flowing northward 

into the Amundsen Sea, a trend indicated by Swithinbank 

and others (2003a, b, 2004). The mass balance of the East 

Antarctic ice sheet is thought by Davis and others (2005) to 

be positive on the basis of the change in satellite-altimetry 

measurements made between 1992 and 2003. On the basis of 

Gravity, Recovery, and Climate Experiment (GRACE) satellite 

measurements of Earth’s gravity from 2002 to 2005, Velicogna 

and Wahr (2006) concluded that the mass of the Antarctic ice 

sheet decreased during the period of measurement, and that the 

West Antarctic ice sheet accounted for most of the loss of ice. 

Rignot and others (2008) studied loss of ice from the Antarctic 

ice sheet on the basis of regional climate modeling and 

satellite interferometric synthetic-aperture radar measurements 

acquired during the period between 1992 and 2006. They 

concluded that ice in East Antarctica is at near-equilibrium or 

has a slightly negative mass balance; ice in West Antarctica, 

including the Antarctic Peninsula, has a negative mass 

balance.

Measurement of changes in area and mass balance 

of the Antarctic ice sheet was given a very high priority in 

recommendations by the Polar Research Board of the National 

Research Council (1986), in subsequent recommendations 

by the Scientific Committee on Antarctic Research (SCAR) 

(1989, 1993), and by the National Science Foundation’s 

(1990) Division of Polar Programs. On the basis of these 

recommendations, the U.S. Geological Survey (USGS) 

decided that the archive of early 1970s Landsat 1, 2, and 3 

Multispectral Scanner (MSS) images of Antarctica and the 

subsequent repeat coverage made possible with Landsat 

and other satellite images provided an excellent means 

of documenting changes in the cryospheric coastline of 

Antarctica (Ferrigno and Gould, 1987). Although changes 

in the areal extent of the Antarctic ice sheet are not directly 

related to changes in mass balance, the two are related, and 

the analysis of the changing coastline can yield important 

information. The availability of this information provided 

the impetus for carrying out a comprehensive analysis of the 

glaciological features of the coastal regions and changes in 

ice fronts of Antarctica (Swithinbank, 1988; Williams and 

Ferrigno, 1988). The project was later modified to include 

Landsat 4 and 5 MSS and Thematic Mapper (TM) images, 

RADARSAT images, and in some areas, aerial photography, 

NOAA AVHRR (National Oceanic and Atmospheric 

Administration, Advanced Very High Resolution Radiometer),

MODIS (Moderate Resolution Imaging Spectroradiometer),

1

U.S. Geological Survey, 926A National Center, Reston, VA 20192–0002.

2

Scott Polar Research Institute, University of Cambridge, Lensfield Road, 

Cambridge CB2 1ER, United Kingdom.

3

U.S. Geological Survey, 384 Woods Hole Road, Woods Hole, MA 

02543–1598.
2 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

and Landsat 7 Enhanced Thematic Mapper Plus (ETM+) 

data to compare changes that occurred during a 20- to 25- or 

30-year time interval (or longer where data were available, 

as in the Antarctic Peninsula). The results of the analysis are 

being used to produce a digital database and a series of USGS 

Geologic Investigations Series Maps (I–2600) (Williams and 

others, 1995; Ferrigno and others, 2002, 2005, 2006, 2007, 

2008, and 2009; Swithinbank and others, 2003a,b, 2004; 

and Williams and Ferrigno, 2005) (available online at http://

www.glaciers.er.usgs.gov). Table 1 lists the USGS Geologic 

Investigations Series coastal-change and glaciological maps of 

Antarctica that have been published to date.

Objectives

The coastal-change and glaciological mapping project has 

five primary objectives:

1. to determine coastline changes that have occurred 

during the past three decades, or longer where additional information exists;

2. to establish an accurate baseline series of 

1:1,000,000-scale maps (fig. 1) that defines, from the 

analysis of Landsat and other satellite images, the 

glaciological characteristics (for example, floating 

ice, grounded ice, and so forth) of the coastline of 

Antarctica during three main time intervals: (1) early 

1970s (Landsat 1, 2, or 3), (2) middle 1980s to early 

1990s (Landsat 4 or 5), and (3) late 1990s to early 

2000s (RADARSAT or Landsat 7 ETM+);

3. to determine velocities of outlet glaciers, ice streams, 

and ice shelves, and the position of the grounding 

line, from analysis of Landsat images and other 

sources;

Table 1. Coastal-change and glaciological maps of Antarctica at 1:1,000,000 scale, published to date.

[Information on ordering published maps can be obtained by calling the U.S. Geological Survey at 1-888-ASK-USGS or by visiting the USGS online at 

http://www.usgs.gov/pubprod]

As shown on 

index map 

Map number Map name References (see References Cited) URL for online access

A

B

C

D

E

F

G

H

I

I–2600–A

I–2600–B

I–2600–C

I–2600–D

I–2600–E

I–2600–F 

(2d ed.)

I–2600–G

I–2600–H

I–2600–I

Trinity Peninsula and South 

Shetland Islands

Larsen Ice Shelf

Palmer Land

Ronne Ice Shelf

Eights Coast

Bakutis Coast

Saunders Coast

Northern Ross Ice Shelf

Ross Island

Ferrigno and others (2006)

Ferrigno and others (2008)

Ferrigno and others (2009)

Ferrigno and others (2005)

Swithinbank and others (2004)

Swithinbank and others (2003b)

Swithinbank and others (2003a)

Ferrigno and others (2007)

This report

http://pubs.usgs.gov/imap/2600/A

http://pubs.usgs.gov/imap/2600/B

http://pubs.usgs.gov/imap/2600/C

http://pubs.usgs.gov/imap/2600/D

http://pubs.usgs.gov/imap/2600/E

http://pubs.usgs.gov/imap/2600/F

http://pubs.usgs.gov/imap/2600/G

http://pubs.usgs.gov/imap/i-2600-h

http://pubs.usgs.gov/imap/2600/I

Figure 1. Index map of the planned and published 1:1,000,000-

scale coastal-change and glaciological maps of Antarctica. Ross 

Island area map is shaded. Maps published to date are indicated 

by letter and described in table 1. They are available printed and 

online; see table 1 for more information.

4. to compile a comprehensive inventory of named 

(from published maps) and unnamed (from analysis 

of Landsat images) outlet glaciers and ice streams 

in Antarctica that are mappable from Landsat and 

other satellite images or from ancillary sources (for 

example, maps, gazetteers, digital databases, and so 

forth) (Swithinbank, 1980, 1985; Alberts, 1981, 1995; 

National Science Foundation, 1989; British Antarctic 

Survey and others, 1993);
5. to compile a 1:5,000,000-scale map of Antarctica 

derived from the 1:1,000,000-scale maps. Each 

1:1,000,000-scale map, apart from the three sheets 

covering the Antarctic Peninsula, extends to the 

southernmost nunatak within each map area or to 

the southernmost extent of Landsat images (about 

lat 81.5o S.). The coverage area of some maps (for 

example, those covering the Ronne and Filchner Ice 

Shelves) was extended farther south to encompass the 

entire ice shelf.

Sources

Most of the earlier maps in the Coastal-Change and 

Glaciological Maps of Antarctica series relied almost 

exclusively on Landsat and other satellite data as the source 

of information. The coverage areas of the Landsat 1, 2, and 

3 MSS images, Landsat 4 and 5 MSS and TM images, and 

Landsat 7 ETM+ images used in the compilation of these 

maps are shown on the index maps contained on the margin 

of each map. Below the index maps, information about each 

image is listed.

On this map, the early Landsat 1 MSS scenes were 

acquired from 1973 to 1974. The Landsat 4 TM images date 

from 1988 to 1990. The Landsat 7 ETM+ images used in the 

analysis of coastline change were digital and date from 2001. 

Other satellite images used were AVHRR data from 2000 and 

2001 and MODIS images from 2002, 2004, and 2005. The 

base for the map was the 1997 RADARSAT image mosaic. 

The 125-meter picture-element (pixel)-resolution 1997 

RADARSAT image mosaic of Antarctica, compiled by The 

Ohio State University’s Byrd Polar Research Center (BPRC), 

was used both as a base for correct geographic position and 

geometric rectification of digitized Landsat imagery and as an 

additional source of coastal-change data.

In addition to incorporating Landsat and other satellite 

imagery, the three Antarctic Peninsula maps (Trinity Peninsula 

area and South Shetland Islands (map I–2600–A), Larsen 

Ice Shelf area (map I–2600–B), and Palmer Land area (map 

I–2600–C)) were compiled utilizing the abundance of current 

and historical vertical and (or) oblique aerial photographs and 

other source material archived by the British Antarctic Survey 

(BAS).

The source material for this map also included the large 

number of topographic and thematic maps produced for the 

Ross Island map area by the USGS and cooperators (see table 

2 and map margin). The maps used for the compilation of this 

publication date from 1962 to 2003.

Although not completed in time to be used in this 

map compilation, the Landsat Image Mosaic of Antarctica 

(LIMA), using about 1,000 Landsat 7 ETM+ images acquired 

between 1999 and 2006 (USGS, 2007), was produced in a 

recent cooperative project between the USGS, the National 

Aeronautics and Space Administration (NASA), the National 

Science Foundation (NSF), and BAS. The mosaic is seamless, 

Introduction 3

virtually cloud-free, and has been corrected for sun angle and 

elevation. It is the most geometrically accurate and highest 

resolution satellite mosaic of Antarctica produced to date and 

is a superb tool for glaciological studies. It is located online at 

http://lima.usgs.gov.

Methodology

The primary steps in the compilation of the Ross Island 

area map are listed and discussed below:

1. Identification of optimum Landsat MSS, TM, or 

ETM+ images for three time intervals (early 1970s, 

middle 1980s to early 1990s, and early 2000s);

2. Manual annotation of glaciological features by SCAR 

Code (Scientific Committee on Antarctic Research, 

1980) or Antarctic Digital Database (ADD) Geocode 

(British Antarctic Survey and others, 1993; ADD 

Consortium, 2007) on 1:500,000-scale transparent 

overlays of Landsat images for both earlier time 

intervals and directly on the computer workstation 

monitor for the 1997 RADARSAT image mosaic and 

Landsat ETM+ images;

3. Positional control of mapped features. Because our 

goal is to produce the most accurate, high-resolution 

printed maps and digital databases of the coastal 

regions of Antarctica, we expended considerable 

thought and research on choosing the optimum 

method of geolocating mapped features. The decision 

was made to georegister the imagery and annotations to the 1997 RADARSAT image mosaic of 

Antarctica, in order to give the most geometrically 

accurate base then available. An added benefit was 

that the RADARSAT mosaic was compiled in polar 

stereographic projection, having a standard parallel at 

lat 71o S.— the same projection selected for the map 

series, making georegistration simpler—with due 

consideration given to scale distortion on map coverage north and south of lat 71o S. (Sievers and Bennat, 

1989). The primary benefit of the polar stereographic 

projection is cartographic continuity between adjacent maps in the coverage provided of the coastal 

regions of Antarctica;

4. Scanning hard-copy photographic images to produce 

400 dots-per-inch (dpi), 256-shade, gray-scale digitized satellite images. The digitized satellite images, 

and those already in digital format, were coregistered 

and geometrically corrected to the RADARSAT 

image mosaic using ERDAS Imagine software. Pass 

points were used for coregistration to geometrically 

fit the scenes to the RADARSAT base;

5. Addition of velocity vectors and geographic placenames; and addition of topographic contours at 
4 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

selected intervals, generated from the BPRC Digital 

Elevation Model data and modified where necessary 

to be congruent with surface features;

6. Description of glaciological features (including the 

position of the grounding line) and analysis of icesurface velocities of selected outlet glaciers and ice 

shelves.

RADARSAT Image Mosaic of Antarctica and its 

Geodetic Accuracy4

The 125-meter picture-element (pixel)-resolution 

RADARSAT image mosaic of Antarctica was used both 

as a base for correct geographic position and geometric 

rectification of digitized Landsat imagery and as an additional 

source of coastal-change data. The RADARSAT image mosaic 

is composed of data recorded from 9 September to 20 October 

1997 and was selected as the most accurate base available at 

the time for geolocating the Landsat imagery; therefore, it 

was considered essential to confirm the published geodetic 

accuracy of the mosaic (±150 m; Noltimier and others, 1999). 

For a description of BPRC procedure for constructing the 

RADARSAT image mosaic, see Jezek, 1998; Norikane and 

others, 1998; and Liu, 1999. The USGS analysis is described 

more fully in earlier coastal-change maps (see USGS Maps 

I–2600–D through H).

Geographic Description

The Ross Island area map is bounded by long 141o E. and 

175° E. and by lat 76° S. and 81o S. Ross Island is named for 

the British explorer James Clark Ross. Ross entered the Navy 

at the age of 11 and spent much of his career exploring first 

the Arctic and then the Antarctic. Between 1839 and 1843, 

he sailed to the Antarctic in his ships, HMS Erebus and HMS 

Terror, sailing farther south than any other known European 

and discovering the sea and the “ice barrier” (ice shelf) that 

are named for him.

The Ross Island area map covers the part of southern 

Victoria Land that includes a small part of the northwestern 

Ross Ice Shelf (fig. 2) (the northern Ross Ice Shelf is described 

on USGS Map I–2600–H), the McMurdo Ice Shelf, part of the 

polar plateau, the Transantarctic Mountains from Byrd Glacier 

to Mawson Glacier, the McMurdo Dry Valleys, northernmost 

Shackleton Coast, Hillary Coast, the southern part of Scott 

Coast, and Ross Island. In the western part of the map area, 

the polar plateau of East Antarctica, once thought to be a 

featureless region, has subtle wavelike surface forms and flow 

traces of glaciers that originate far inland and extend to the 

Figure 2. Location map of Antarctica showing West and East 

Antarctica, the Transantarctic Mountains, the Ross Ice Shelf, and 

the Antarctic Peninsula. The map area of this report is outlined.

coast or into the Ross Ice Shelf. There are numerous outlet 

glaciers. In the northern part of the map area, many glaciers 

drain into the McMurdo Dry Valleys; the rest drain through the 

Transantarctic Mountains into the Ross Sea or are tributaries 

of glaciers that do. In the southern part of the map area, many 

of the glaciers drain into the Ross Ice Shelf, and Byrd Glacier 

is the largest. West of the Transantarctic Mountains are areas 

of blue ice, where drainage of the ice through the mountains 

has been impeded. These blue ice areas, readily identifiable on 

Landsat images, have been determined to be prime areas for 

finding meteorites (Williams and others, 1983; Schutt, 2007). 

In addition, three subglacial lakes have been identified in the 

map area (Siegert, 2002). Because McMurdo Station, the main 

U.S. scientific research station, is located on Ross Island in the 

map area, many of these and other features in the area have 

been studied extensively. In addition, the USGS has produced 

a large number of reconnaissance, topographic, satellite 

image, and orthophoto maps of McMurdo Sound, McMurdo 

Station, Ross Island, Ross Sea, the McMurdo Dry Valleys, and 

northern Victoria Land at a variety of scales to represent the 

area cartographically and support scientific research (see 

table 2).

Glacier Inventory and Glaciological 

Features

Producing a sophisticated glacier inventory of the entire 

continent of Antarctica according to the requirements of the 

World Glacier Monitoring Service (Müller and others, 1977, 

4

Geodetic accuracy determined by J. William Schoonmaker, research geodesist, U.S. Geological Survey (retired).
Coastal-Change Analysis—Discussion of Selected Glaciological Features 5

1978), as part of its ongoing “World Glacier Inventory” 

program, has been impossible with the present state of 

glaciological knowledge about Antarctica (Swithinbank, 

1980). As recently as 2009, the World Glacier Inventory 

Web site hosted by the National Snow and Ice Data Center 

(NSIDC) did not include Antarctic data. However, as more 

remotely sensed data become available, and as more scientific 

interest is focused on Antarctica, more glacier inventories will 

be developed, especially for localized areas. The first glacier 

inventory carried out in Antarctica using the methodology of 

the World Glacier Inventory was done on the northern end 

of the Antarctic Peninsula on James Ross Island by Rabassa 

and others (1982). Braun and others (2001) proposed a 

geographic information system (GIS)-based glacier inventory 

for the Antarctic Peninsula as part of the Global Land Ice 

Measurements from Space (GLIMS) Project (Kieffer and 

others, 2000), and Rau and others (2004) carried out a 

comprehensive GIS inventory of 900 individual glaciers and 

glaciological features in the northern part of the Antarctic 

Peninsula.

Because of the glaciological complexity and the large 

number of unnamed and unidentified glaciers in the map area, 

we have not attempted to compile a comprehensive glacier 

inventory of the unnamed glaciers. Instead, we have compiled 

a list of named glaciers and related glaciological features 

within the Ross Island map area, gathered from published 

maps, the USGS Geographic Names Information System 

(GNIS) database (http://geonames.usgs.gov/antarctic/index.

html), and the SCAR Composite Gazetteer of Antarctica 

(http://data.aad.gov.au/aadc/gaz/scar/). This list is presented in 

table 3.

The map area has an amazing variety of glaciological 

features. There are 323 named glaciers and related 

glaciological features on the map as defined in various 

scientific glossaries (Armstrong and others, 1973, 1977; 

Neuendorf and others, 2005). The named features include 

outlet, valley, and cirque glaciers, and ice shelves, ice 

piedmonts, snowfields, ice fields, icefalls, and glacier tongues 

(table 3).

Coastal-Change Analysis—Discussion 

of Selected Glaciological Features

As would be expected, floating ice fronts, iceberg 

tongues, and glacier tongues are the most dynamic and 

changeable features in the coastal regions of Antarctica. 

On this map, unlike most of the previous maps in this series, 

the ice fronts do not show much change. The positions of the 

ice fronts as observed on the three sets of Landsat imagery 

and on other satellite imagery were mapped and annotated 

with the date for each position. This made it possible to date 

and analyze changes that have occurred. The only noticeable 

change, however, is along the front of the McMurdo Ice 

Shelf, where recession of a few kilometers to as much as 5 km 

occurred between January 1974 and October 1997. As a result, 

the following discussion focuses on the glaciological features 

of the area.

Glaciers that Drain from or through the 

Transantarctic Mountains

Byrd Glacier

Byrd Glacier is one of the largest valley glaciers in the 

world and possibly the most active glacier draining the polar 

plateau of East Antarctica. It has surface velocities of more 

than 800 m a-1, as fast as some surging glaciers. Byrd Glacier 

is more than 180 km long and is 22 km wide at its narrowest 

point (Swithinbank, 1988). It drains an area greater than 1 x 

106 km2 and is the largest single source of ice (more than 18 

km3 a-1) flowing into the western margin of the Ross Ice Shelf. 

Its flow pattern can be followed across the Ross Ice Shelf to 

the Ross Sea. In spite of its size and importance, it was not 

well known or named before 1960 (Swithinbank, 1963). The 

entire length of Byrd Glacier was not successfully imaged 

by moderate-resolution satellite imagery until 1982, when 

Landsat 4 with its more southerly orbit was able to view the 

upper region of the glacier (Swithinbank, 1988).

Because of the fact that Byrd Glacier provides the 

primary outflow for a major part of East Antarctica, studies 

have been made of its current and past behavior to help predict 

its future and to understand its role in influencing the mass 

balance of the entire East Antarctic ice sheet. Work was first 

done on Byrd Glacier as part of the International Geophysical 

Year (IGY). Swithinbank’s measurements, made between 

1960 and 1962, of seven glaciers flowing into the Ross Ice 

Shelf discovered the overwhelming contribution of the outflow 

of Byrd Glacier (Swithinbank, 1963). In 1978 and 1979, 

extensive field studies were carried out on the glacier as part 

of the Byrd-Darwin Glacier project. The studies included 

aerial photography, radio echo sounding, ground-survey ice 

sampling, and ablation measurements (Hughes, 1979; Hughes 

and Fastook, 1981). Brecher (1982) used stereographic vertical 

aerial photographs to photogrammetrically determine surface 

velocities and elevations. He calculated a maximum surface 

velocity of 875 m a-1 well upstream of the glacier mouth. 

All velocities compared well with Swithinbank’s 1960–62 

measurements and with the 1978–79 field measurements. 

Brecher (1962) also compared the 1978–79 aerial photographs 

with aerial photographs acquired in 1960 and 1963; he 

determined that there was no appreciable change in the surface 

elevation during the time interval. Further surface-velocity 

measurements were made by Lucchitta and Ferguson (1986) 

using Landsat MSS data from January 1974 and November 

1983. Their average velocities were between 750 and 800 m 

a-1, about the same as the earlier measurements. In contrast, 

recent ice-velocity measurements acquired using 2000–2001 

Advanced Spaceborne Thermal Emission and Reflectance 
6 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

(ASTER) imagery by Stearns and Hamilton (2005) showed 

substantial deceleration of Byrd Glacier. Parts of the glacier 

that had been flowing at 850 m a-1 in 1978–79 were flowing 

at 650 m a-1 in the ASTER data, indicating the flow of this 

glacier is very dynamic and changeable over time.

Models to describe the dynamics of Byrd Glacier were 

made using the 1978–79 field data and radio-echo sounding 

data. Reusch and Hughes (2003) suggest that Byrd Glacier 

may be undergoing rapid changes based on evidence of ice 

flux, information on basal melting (Rignot and Thomas, 2002), 

and a position for the grounding line (Rignot and Thomas, 

2002) that is 20 km farther inland than where it was located 

by Hughes and Fastook (1981). Kenneally and Hughes (2004) 

suggest that if the grounding line is retreating upglacier, this 

eventually could lead to the drawdown of ice from the interior 

of East Antarctica.

Darwin Glacier

Darwin Glacier, more than 90 km long and 3 km wide, 

is a large glacier that flows from the Darwin Mountains into 

the Ross Ice Shelf. The lower part of the glacier was first 

mapped in the early 1900s by the British National Antarctic 

Expedition. The glacier was visited by the Commonwealth 

Trans-Antarctic Expedition in 1956–58. In 1978–79, the ByrdDarwin Glacier field project visited Darwin Glacier. Although 

most of the focus of the project was on Byrd Glacier, icesurface-velocity measurements were made on Darwin Glacier 

and indicated a maximum surface velocity of 100 m a-1

(Hughes, 1979; Hughes and Fastook, 1981).

Hatherton Glacier

Hatherton Glacier is a large glacier, approximately 3 km 

wide and more than 60 km long. It is a tributary to Darwin 

Glacier, which it joins after flowing through the Transantarctic 

Mountains. Both Darwin and Hatherton Glaciers are ice 

starved, with little to no flow from the polar plateau and little 

contribution to the Ross Ice Shelf. A modeling study of the 

response of Hatherton Glacier to Ross Ice Sheet groundingline retreat in the Holocene was carried out by Anderson and 

others (2004) to contribute to the understanding of present and 

future grounding-line retreat of the West Antarctic ice sheet.

Mulock Glacier

Mulock Glacier is a large glacier, more than 80 km long 

and about 12 km wide, that drains the polar plateau. Less 

than half as wide as Byrd Glacier, it is still considered an 

important outlet glacier. Its surface elevation is 1,400 m at 

the plateau and decreases to 100 m where it joins the Ross Ice 

Shelf (Swithinbank, 1988). Swithinbank (1963) made surfacevelocity measurements during 1960–62 to assess the overall 

contribution of several outlet glaciers to the total regime of the 

Ross Ice Shelf. The surface velocity of Mulock Glacier was 

measured at about 390 m a-1 near its mouth, contributing 5.6 

km3 a-1 of ice to the shelf. Scambos and others (http://nsidc.

org/data/velmap/ross_shelf/ross_nw/ross_nw_vel.html) used 

Landsat imagery from 1989 to calculate ice-surface velocity. 

Their results were similar to the earlier measurements, with 

velocities at the grounding line about 350 to 400 m a-1, 

increasing to more than 700 m a-1 as the glacier moved into the 

Ross Ice Shelf.

Skelton Glacier

Skelton Glacier is a large glacier flowing from Skelton 

Névé, from which it gets most, if not all, of its nourishment, 

into the Ross Ice Shelf. It is about 130 km long, and its 

maximum thickness is 1,450 m. Its surface drops from 2,200 

m on the plateau to 100 m at the grounding line. The glacier 

was the route for traveling from the Ross Ice Shelf to the polar 

plateau by the Commonwealth Trans-Antarctic Expedition in 

1956–58 and the Victoria Land Traverse in 1958– 59. During 

the latter ascent, seismic, gravity, magnetic, and glaciological 

studies were made. The glaciological studies included icethickness and ice-movement measurements. At the mouth of 

the glacier, the ice thickness ranged from 490 to 600 m, the 

ice-surface velocity averaged about 89 m a-1, and the discharge 

to the shelf was only 0.8 km3 a-1 of ice (Wilson and Crary, 

1961). As a result, Skelton Glacier has very little effect on the 

flow of the ice shelf. During the 1960–61 geophysical traverse 

from McMurdo Station to the South Pole, Skelton Glacier was 

also the route chosen to access the polar plateau.

Koettlitz Glacier

Koettlitz Glacier drains from Koettlitz Névé in the 

Transantarctic Mountains and flows between Brown Peninsula 

and the mainland, entering McMurdo Sound near Cape 

Chocolate. Koettlitz Glacier is more than 75 km long, and its 

tongue is afloat for at least 25 km. It has received scientific 

attention since the days of Scott’s expeditions (1910–13) 

because of the fish and marine invertebrates found on its 

surface. The hypothesis that the surface distribution of marine 

fauna was explained by freezing of marine organisms to the 

base of the ice shelf (basal freezing) and gradual migration 

upward to the surface (surface ablation) was confirmed by 

Gow and Epstein (1972). Gow and Govoni (1994) used map 

data, field observations, and remotely sensed data to observe 

the retreat of the ice front from 1910–13 to 1992; they 

estimated that more than 300 km2

 of ice had calved off the 

glacier tongue during that 80-year period.

Erebus Glacier Tongue

A small but distinctive feature on the map, due to its 

serrated edges, is the Erebus Glacier Tongue, the extension 

of Erebus Glacier into Erebus Bay. Erebus Glacier Tongue is 
Coastal-Change Analysis—Discussion of Selected Glaciological Features 7

unusually long (14 km) and unusually narrow, averaging only 

about 1.5 km in width (Delisle and others, 1989). The tongue 

was originally mapped by the British National Antarctic 

Expedition under Scott (1901–04) and has been intensively 

studied with radio-echo sounding and other techniques since 

1967. It is floating for about 13.5 km of its length (Delisle 

and others, 1989). According to Holdsworth (1974, 1982), 

it is 350 m thick at the grounding line and thins to 120 m at 

its seaward end. Holdsworth (1974) measured an ice-surface 

velocity at the seaward end of 165 m a-1, but Delisle and others 

(1989) cited an average velocity of 140 m a-1. Holdsworth 

(1974) determined that the glacier tongue has a calving 

recurrence interval of 30 years, but according to Delisle and 

others (1989), the last calving event occurred about 1944 

and was long overdue. The delay in calving may have been 

due, in part, to buffering by the sea ice that surrounds the 

glacier tongue.

McMurdo Dry Valleys

The McMurdo Dry Valleys region on this map, extending 

roughly from lat 76.5o S. to 78.5o S. and from long 160o 

E. to 164.5o E., is an area of about 16,000 km2, of which 

approximately 2,000 km2 is essentially snow free (Chinn, 

1988). The three major, mostly ice-free valleys are Taylor, 

Wright, and Victoria Valleys. There are three main types of 

glaciers in the region. Outlet glaciers from the East Antarctic 

ice sheet enter the valleys from the west. The mountain ranges 

between the valleys support alpine glaciers, and piedmont 

glaciers are located along the coast (Chinn, 1988). Chinn 

(1988) thought and Fountain and others (2006) showed that 

the alpine glaciers were approximately in equilibrium. Glacier 

velocities in the area are typically very slow, generally 1 m a-1

or less, with the maximum of 3 m a-1 measured on Meserve 

Glacier (Chinn, 1988; Fountain and others, 2006). But Chinn 

(1998) stated that if it is taken into consideration that the 

flow and ablation regimes of the McMurdo Dry Valleys’ 

glaciers are two orders of magnitude slower than those of 

temperate glaciers, then the glaciers actually are fluctuating 

as dynamically as temperate glaciers. Because the McMurdo 

Dry Valleys are so close to McMurdo Station, many studies 

have been carried out on the glaciers there. Some of the 

more comprehensive include Chinn (1980, 1985, 1998), 

Fountain and others (1998, 2004, 2006), and Fountain and 

Lyons (2003). Interesting work was done by MacClune and 

others (2003), who considered that the conditions of high 

sublimation, low melting, and dust accumulation made the 

glaciers in the McMurdo Dry Valleys terrestrial analogs for 

Martian ice caps.

Icebergs

Large icebergs have not calved in the map area recently, 

but icebergs that have calved and drifted westward from the 

eastern part of the Ross Ice Shelf have impacted the wildlife 

on Ross Island and impeded access to McMurdo Station. 

In the last decade, several very large icebergs calved from 

the front of the eastern part of the Ross Ice Shelf (Ferrigno 

and others, 2007). On 17 March 2000, one of the largest 

tabular icebergs ever recorded was seen; it was named B-15. 

It calved from west of Roosevelt Island along rifts that had 

been observed on satellite imagery for several years (Lazzara 

and others, 1999). It was 295 km long, 37 km wide, and had 

an area of about 10,000 km2

. Soon afterward, several new 

icebergs were formed by the breaking of B-15 into smaller 

pieces (B-15A, B, C, and D) and by the collision of B-15 with 

the ice shelf (B-16, -17, -18, and -19, and C-16). B-15A, the 

largest remnant of the original B-15, and C-16 drifted west 

until they collided with Ross Island in December 2001 and 

December 2000, respectively, where they remained until at 

least October 2003. The icebergs disrupted ocean circulation, 

shipping, and marine life. MacAyeal and others (2003) placed 

automatic weather stations, ice-sounding radar, seismometers, 

and tracking devices on B-15A and C-16 for detailed 

monitoring and to model the effects of future climate change 

on the ice shelves of Antarctica. See Ferrigno and others 

(2007) for additional discussion of the calving of these and 

other icebergs from the Ross Ice Shelf.

Ice Cores

Antarctic ice cores are a unique and powerful resource 

for studying climate change (Wolff, 2005). Both shallow 

and deep cores have yielded important information in many 

parts of the continent. The International Trans-Antarctic 

Scientific Expedition (ITASE), planned for the continentwide collection and interpretation of environmental data, has 

included ice-core drilling in its program to reconstruct the last 

approximately 200 years of climate change, or longer where 

data are available (http://www2.umaine.edu/itase/). Since 

1968, deep ice cores have been drilled in Antarctica that have 

yielded information on previous climate for several hundreds 

of thousands of years. In 1968, the first core to extend through 

the ice sheet and reach bedrock was drilled at Byrd Station 

(lat 80° S., long 119.5° W.). It was 2,191 m long and was 

dated at more than 50,000 years (Hammer and others, 1994). 

The 3,623-m Vostok core (drilled in different intervals from 

1970 to 1998) gave information from the last four glacialinterglacial cycles, extending back about 420,000 years (Petit 

and others, 1999). The first Dome Fuji (lat 77°19 ́ S., long 

39°42 ́ E.) deep ice core, drilled in 1995 and 1996, was 2,500 

m long and extended back 340,000 years (Watanabe and 

others, 1999; Kawamura and others, 2007). Another deep core 

from Dome Fuji, drilled from 2003 to 2007 and 3,035 m long, 

may cover as many as 720,000 years (Motoyama, 2007). The 

Dome Charlie (C) ice core (lat 75°06 ́ S., long 123°24 ́ E.) 

has reached the oldest ice to date. Drilled from 1999 to 2004, 

it was 3,270 m long and reached ice extending back more 

than 800,000 years and covering at least eight glacial cycles 

(EPICA, 2004).
8 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

On this map sheet, Taylor Dome (lat 77°40 ́ S., long 

157°40 ́ E.), which receives ice from Dome Charlie and 

drains to the Ross Sea through Scott Coast (Frezzotti and 

others, 2000), is the location of an ice-drilling project that 

successfully reached bedrock at a depth of 554 m. The project 

was started in 1990–91, and drilling, which was begun in 

1991–92, was completed in the 1993–94 season. The Taylor 

Dome ice core, containing a paleoclimatic record longer than 

130,000 years, was only the second (after Vostok) to provide 

a stratigraphically undisturbed record through the entire 

last glacial cycle. Because the core is relatively shallow, it 

has provided excellent CO2

 and δ 13C (proxy temperature) 

measurements (http://depts.washington.edu/isolab/taylor). 

Reviews of the project and results are in Morse and others 

(1999) and Steig and others (2000).

Blue-Ice Areas and Meteorites

Areas of bare glacier ice, turquoise-blue in color, 

contrasting sharply with the more extensive white snow cover, 

occur in many parts of Antarctica and are called “blue ice,” 

a term first used by the Swedish glaciologist Valter Schytt 

(1961) during the 1944–52 Norwegian-British-Swedish 

Expedition to Queen Maud Land. Blue ice is found primarily 

near coastal mountains and nunataks but can appear in the 

interior within the main flow of the ice sheet. Blue-ice areas 

became linked with the search for meteorites in 1970. From 

earliest exploration until 1969, only four meteorites had been 

found in Antarctica, all during overland traverses, and it was 

thought that there were extremely limited opportunities for 

finding meteorites in Antarctica. During the 1969–70 Antarctic 

field season, Japanese scientists found nine meteorites in 

a blue-ice area of the Queen Fabiola (Yamato) Mountains 

(Yoshida and others, 1971) and many more in succeeding 

years. This unexpected discovery suggested that blue-ice 

areas might be a rich source of meteorites. In 1975, the 

United States inaugurated a search program (Antarctic Search 

for Meteorites, ANSMET) that first focused in the blue-ice 

areas around the Allan Hills in cooperation with Japanese 

scientists; eleven meteorites were found (Cassidy, 1977). The 

successful search soon expanded to other areas and found 

increasing numbers of specimens. Since then, international 

search teams have located about 35,000 specimens in 

Antarctica (Schutt, 2007).

Blue ice occurs in areas of low accumulation (less 

snowfall), high ablation, high wind speed (removes snow and 

increases ablation), and slow horizontal motion (Annexstad, 

1982), where the ice movement is completely or partly 

blocked by subglacier or subaerial mountain ranges. A 

meteorite fall is a rare occurrence, and slow ice flow against 

a blockage concentrates meteorites on an ablating surface. 

Low temperatures also slow the deterioration of meteorites 

that are not in chemical equilibrium at the Earth’s surface 

(Cassidy and others, 1992). The co-location of meteorites 

and blue ice has yielded information for both the meteorite 

and glaciological scientific communities. Blue-ice areas have 

also been investigated for use as aircraft landing sites for 

wheeled aircraft (Mellor and Swithinbank, 1989; Swithinbank, 

1989, 1991). The idea has proved valid and has been used 

and developed by private and government entities of several 

countries.

It was recognized early in the search for meteorites that 

identification of blue-ice areas, using aerial reconnaissance or 

inspection of satellite imagery, could greatly aid the search, 

and a suggestion was made to compile a thematic map of the 

continent using satellite imagery (Williams and others, 1982, 

1983). The Japanese produced early maps of the meteorite 

locations in the Yamato Mountains and the Allan Hills (Yanai, 

1983, 1984). A concerted effort to map meteorite locations 

grew out of the need to document, present, and maintain 

ANSMET location data (Antarctic Meteorite Location and 

Mapping Project, AMLAMP) (Schutt and others, 1989, 1993). 

Thematic maps were produced until 1994, but currently 

mapping is being done in the ESRI ArcGIS environment 

(Schutt, 2007).

Meteorites have been found in East Antarctica in 

the Yamato and Sør Rondane Mountains and along the 

Transantarctic Mountains. The greatest number have been 

found in the Yamato and Sør Rondane Mountains and 

the nearby area (more than 16,500 meteorites as of 2008, 

according to Japan’s National Institute of Polar Research, 

Antarctic Meteorite Research Center Web site (http://www.

nipr.ac.jp/english/r_centers/t04_amrc.html)), but the greatest 

extent is along the Transantarctic Mountains, where the flow 

of the East Antarctic ice sheet has been obstructed. Several 

of the sites are located on this map sheet. The Allan HillsDavid Glacier region (David Glacier is about 75 km north of 

the map area) includes numerous meteorites from the Allan 

Hills, Elephant Moraine, and Reckling Moraine areas and 

has yielded approximately 3,400 meteorite specimens. The 

McMurdo Dry Valleys region has yielded a few meteorites, 

and the Darwin-Byrd Glacier region has yielded more than 

1,100 specimens, mostly from the Meteorite Hills (Schutt 

2007). Harvey (2003) gave a comprehensive discussion of the 

origin and significance of Antarctic meteorites.

Subglacial Lakes

Subglacial lakes were first recognized in Antarctica in 

airborne radio-echo sounding records in the late 1960s by 

Robin and others (1970). Oswald and Robin (1973) counted 

17 of these lakes at the base of the ice sheet beneath several 

thousand meters of ice. Since then, new data and re-evaluation 

of older data have increased the number of recognized lakes 

to 77 (Siegert and others, 1996), and 145 (Siegert and others, 

2005). It is worth noting that although the data do not cover 

the whole continent, subglacial lakes have been found in 

much of the data, suggesting they exist continent-wide. The 

lakes range in size from about 500 m in length to the largest 

known lake, Vostok Subglacial Lake. Vostok, first described 
References Cited 9

by Kapitsa and others (1996), has been studied intensively 

and is now recognized to have maximum dimensions of 

250 km by 80 km and a total area of 14,000 km2

 (Siegert 

and others, 2005). Most subglacial lakes are located in the 

interior of the ice sheet where surface slopes, ice velocity, and 

surface accumulation are low (Siegert, 2002). Dowdeswell 

and Siegert (2002) divided subglacial lakes into three types 

based on location: (1) lakes in subglacial basins in the icesheet interior, (2) lakes on the flanks of subglacial mountains, 

and (3) lakes near the onset region of enhanced glacier flow. 

Sixteen lakes fall into the last category and of these, three 

occur near the onset of fast flow into Byrd Glacier (Siegert, 

2002), the glacier that is a major glaciological feature on this 

map. Subglacial lakes, especially Vostok Subglacial Lake, 

are of interest because of the possible inclusion of unique life 

forms that may indicate if life can exist in harsh conditions in 

other parts of the solar system and help explain the processes 

that triggered the evolutionary explosion on Earth. Also their 

presence may help decipher the geologic history of Antarctica, 

including the location and dynamics of paleo-ice sheets 

(Bell and Karl, 1998).

Summary

The analysis of Landsat 1 MSS images (1973 to 1974), 

Landsat 4 TM images (1988 to 1990), Landsat 7 ETM+ 

images (2001), and other satellite imagery and historical 

data of the Ross Island area made it possible to identify and 

describe glaciological features. Little noticeable change has 

occurred in the ice fronts on the map, with the exception of 

overall recession in the McMurdo Ice Shelf area of up to 5 km 

between 1974 and 1997. Therefore the discussion is focused 

on a review of selected glaciers that flow from or through the 

Transantarctic Mountains including Byrd, Darwin, Mulock, 

Skelton, and Koettlitz Glaciers. The following glaciological 

topics are also reviewed: the Erebus Glacier Tongue, 

investigations in the McMurdo Dry Valleys, and iceberg 

calving, ice cores, subglacial lakes, and the relation of blue ice 

to accumulation of meteorites.

Acknowledgments

We would like to acknowledge the outstanding support 

provided for the preparation of this map by numerous 

individuals. Charles Swithinbank’s participation in the project 

was made possible by the much-appreciated support of Jerry 

C. Comati, Chief, Environmental Sciences Branch, U.S. Army 

Research, Development, and Standardization Group (London, 

United Kingdom) of the U.S. Army Materiel Command. We 

are indebted to Dann S. Blackwood, USGS (Woods Hole, 

Mass.) and the late Lewis V. Thompson, USGS (Reston, 

Va.) for assistance with custom photographic processing of 

Landsat images. For the map series, James R. Estabrook, 

USGS (Reston, Va.) provided superb and thorough map and 

text edits, and D. Paul Mathieux, USGS (Reston, Va.) created 

excellent computer graphics. John Splettstoesser and Andrew 

Fountain provided very helpful reviews. Funding for the 

project was provided by the USGS commitment to the multiFederal agency U.S. Climate Change Science Program.

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16 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

Table 2. Topographic, satellite image, and photo maps in the Ross Island map area, produced by the USGS and cooperators.—

Continued

Name Publication Date

1:250,000-Scale Topographic Reconnaissance Series

Cape Selborne

Carlyon Glacier

Convoy Range

Franklin Island

Mount Discovery

Mount Harmsworth

Mount Olympus

Ross Island

Taylor Glacier

Turnstile Ridge

1966

1966

1965, revised 1988

1965

1965, revised 1988

1965, revised 1988

1966

1960, revised 1970

1965, revised 1988

1966, revised 1988

1:250,000-Scale Satellite Image Maps

Churchill Mountains

Convoy Range

Darwin Mountains

Mount Harmsworth

Mount Joyce

Ross Island

South Ross Sea Region

2003

1974 (printed 1989)

2002

1974 (printed 1989)

1974 (printed 1989)

1975 (printed 1989)

1999

1:100,000-Scale Satellite Image Maps

Byrd Névé

Convoy Range

Darwin Glacier

McMurdo Dry Valleys

Mount Discovery

Nicholson Peninsula

Ross Island and McMurdo Sound

Skelton Névé

Turnstile Ridge

2003

2000

2001

1995

1999

2003

2000

2000

2001

1:50,000-Scale Topographic Series

Alatna Valley (co-op with New Zealand)

Beacon Valley (co-op with New Zealand)

Cambridge Glacier (co-op with New Zealand)

Cape Chocolate (co-op with New Zealand) 

Cape Roberts (co-op with New Zealand)

Cathedral Rocks (co-op with New Zealand)

Debenham Glacier (co-op with New Zealand)

Flagship Mountain (co-op with New Zealand)

Granite Knolls (co-op with New Zealand)

Joyce Glacier (co-op with New Zealand)

In preparation

1993

In preparation

1993

In preparation

1993

In preparation

In preparation

1993

1997
Appendix—Tables 2 and 3 17

Table 2. Topographic, satellite image, and photo maps in the Ross Island map area, produced by the USGS and cooperators.—

Continued

Name Publication Date

1993

1977

1977

1977

1977

1977

1977

1997

In preparation

1997

1997

In preparation

In preparation

In preparation

1997

1997

1997

1977

1977

In preparation

n.d. [2005]

In preparation

2002

In preparation

n.d. [2005]

1999

2002

2001

2001

2001

In preparation

In preparation

2002

2002

In preparation

In preparation

1991

1996, 2d ed. 2000

1:50,000-Scale Topographic Series—Continued

Knobhead (co-op with New Zealand)

Labyrinth

Lake Bonney

Lake Brownworth

Lake Fryxell

Lake Vanda

Marble Point 

Marshall Valley (co-op with New Zealand)

Mount Endeavour (co-op with New Zealand)

Mount Huggins (co-op with New Zealand)

Mount Lister (co-op with New Zealand)

Mount Mahony (co-op with New Zealand)

Mount Whitcombe (co-op with New Zealand)

Skew Peak (co-op with New Zealand)

The Pyramid (co-op with New Zealand)

The Spire (co-op with New Zealand)

Twin Rocks (co-op with New Zealand)

Victoria Upper Lake

Webb Lake

Wyandot Ridge (co-op with New Zealand)

1:25,000-Scale Satellite Image Maps

Airdevronsix Icefalls

Beacon Heights

Cape Crozier

Cavendish Rocks

Dais

Denton Glacier

Hut Point Peninsula

Lake Fryxell

Marble Point

Matterhorn

Miers Valley

Mount Bastion

Mount Bird

Mount Erebus

Mount Kowalczyk

Victoria Valley

Miscellaneous Scale Satellite Image Maps

I-2284 Antarctica, 1:5,000,000

I-2560 Antarctica, 1:5,000,000
18 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

Table 2. Topographic, satellite image, and photo maps in the Ross Island map area, produced by the USGS and cooperators.—

Continued

Name Publication Date

Miscellaneous Scale Satellite Image Maps—Continued

RADARSAT Image Map of Antarctica, 1:5,000,000

Victoria Land Coast, 1972–73, 1:1,000,000

McMurdo Sound, 1972–74, 1:1,000,000

McMurdo Sound Region, 1:500,000

McMurdo Sound Region, 1:250,000

2003

1976

1976

1973 (printed 1975)

1973

Miscellaneous Scale Photomaps

Hut Point Peninsula, 1:13,500 

McMurdo Station, 1:2,500

McMurdo Station, 1:1,800

McMurdo Station, 1:1,560 

McMurdo Station, USA – Scott Base, NZ, 1:8,000

1983 (printed 1985)

1983 (printed 1985)

1996

2001

2000

Miscellaneous Other Maps

Ross Ice Shelf, 1:2,188,000 (sketch map)

Ross Ice Shelf, 1:1,000,000 (sketch map)

McMurdo Sound, 1:1,000,000 International Map of the World series

Ross Island and vicinity, 1:250,000 Topographic

Ice-Free Valleys, Victoria Land, 2 sheets, 1:100,000 Topographic, 

USGS Open-File Report 84–303

Skelton Glacier, 1:100,000 Topographic, 

USGS Open-File Report 84–304

Wright Valley Labyrinth Area, 1:20,000 Topographic, 

USGS Open-File Report 84–302

Cape Crozier, Ross Island, 1:4,800 Topographic, 

USGS Open-File Report 84–301

1980 (compiled 1972)

1972

1974

1986

1984 (compiled 1962)

1984 (compiled 1962)

1984 (compiled 1965)

1984 (compiled 1963)
Appendix—Tables 2 and 3 19

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Adams Glacier 780700S 1633800E

Adélie Glacier 771300S 1663000E

Aiken Glacier 773800S 1632400E

Airdevronsix Icefalls 773100S 1602200E

Albatross Glacier 771700S 1663100E

Alberich Glacier 773600S 1613600E

Albrecht Penck Glacier 764000S 1622000E

Alley Glacier 795800S 1580500E

Allison Glacier 781600S 1615500E

Amos Glacier 774900S 1633900E

Amphitheatre Glacier 781700S 1630400E

Ant Hill Glacier 784900S 1613000E

Anu Whakatoro Glacier 771725S 1614200E

Atka Glacier 764100S 1613300E

Aurora Glacier 773700S 1673800E

Bachtold Glacier 770730S 1620000E

Ball Glacier 780300S 1625000E

Barne Glacier 773600S 1662600E

Baronick Glacier 783600S 1615000E

Bartley Glacier 773200S 1621300E

Bartrum Glacier 794400S 1584400E

Baxter Glacier 764000S 1615100E

Benson Glacier 764900S 1621200E

Beowulf Glacier 773800S 1614900E

Bertoglio Glacier 791800S 1602000E

Biker Glacier 771200S 1600700E

Bindschadler Glacier 775800S 1620900E

Blackwelder Glacier 775600S 1641200E

Blankenship Glacier 775900S 1614500E

Blue Glacier 775000S 1641000E

Bol Glacier 775200S 1623400E

Bonne Glacier 775300S 1634900E

Borns Glacier 774700S 1620100E

Bowden Glacier 780800S 1630700E

Bowers Piedmont Glacier 774300S 1641800E

Brecher Glacier 804200S 1572800E

Brier Icefalls 801500S 1553600E

Bryan Glacier 772415S 1605545E

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Burrows Glacier 780200S 1635600E

Byrd Glacier 802000S 1590000E

Byrd Névé 810000S 1540000E

Calkin Glacier 774600S 1621700E

Cambridge Glacier 765700S 1603100E

Canada Glacier 773700S 1625900E

Carleton Glacier 780100S 1623000E

Carlyon Glacier 793400S 1595000E

Cassidy Glacier 774600S 1600900E

Cassini Glacier 775300S 1634800E

Catspaw Glacier 774300S 1614200E

Cavendish Icefalls 774900S 1612000E

Cerberus Glacier 772700S 1615400E

Chattahoochee Glacier 763400S 1604200E

Chinn Glacier 772800S 1621500E

Circle Icefall 793800S 1563000E

Clark Glacier 772500S 1622500E

Cleveland Glacier 765500S 1620100E

Clio Glacier 772600S 1620000E

Cocks Glacier 784100S 1620000E

Comberiate Glacier 782100S 1621400E

Commanda Glacier 773000S 1625600E

Commonwealth Glacier 773500S 1631900E

Condit Glacier 775200S 1624800E

Conrow Glacier 773400S 1620700E

Cooper Snowfield 805600S 1584000E

Cotton Glacier 770700S 1614000E

Covert Glacier 775400S 1630400E

Cranfield Icefalls 795600S 1584000E

Creagh Glacier 780100S 1611000E

Creagh Icefall 780200S 1610800E

Crescent Glacier 774000S 1631400E

Crisp Glacier 771200S 1621200E

Cycle Glacier 771200S 1601000E

Dahe Glacier 771500S 1620200E

Dale Glacier 781700S 1620200E

Darkowski Glacier 775200S 1622500E

Darwin Glacier 795300S 1590000E
20 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Darwin Névé 793000S 1550000E

Debenham Glacier 771000S 1623800E

Deception Glacier 783300S 1583300E

Decker Glacier 772800S 1624700E

Delinski Glacier 772900S 1602600E

Delta Glacier 784200S 1612000E

Denton Glacier 772900S 1623600E

Descent Glacier 775100S 1625200E

DeVries Glacier 802000S 1573000E

Dewdrop Glacier 770100S 1622200E

Diamond Glacier 795100S 1590000E

Dilemma Glacier 784500S 1612500E

Discovery Glacier 782000S 1643000E

Doran Glacier 774300S 1624000E

Double Curtain Glacier 773900S 1633100E

Dromedary Glacier 781800S 1631000E

Dun Glacier 774800S 1621400E

Eady Ice Piedmont 783100S 1652000E

Eastwind Glacier 773700S 1681600E

Emmanuel Glacier 775400S 1620500E

Endeavour Piedmont Glacier 772300S 1664000E

Entrikin Glacier 804900S 1600000E

Enyo Glacier 772900S 1620000E

Eos Glacier 772800S 1621000E

Erebus Glacier 774100S 1670000E

Erebus Glacier Tongue 774200S 1664000E

Evans Piedmont Glacier 764400S 1624000E

Evteev Glacier 785700S 1611200E

Exodus Glacier 795000S 1562200E

Fang Glacier 772900S 1670600E

Fastook Glacier 790200S 1564500E

Fenwick Glacier 771633S 1614135E

Ferguson Glacier 773100S 1625600E

Ferrar Glacier 774600S 1630000E

Ferrigno Glacier 780800S 1615900E

Fireman Glacier 774700S 1601600E

Flight Deck Névé 764700S 1613000E

Foggydog Glacier 794700S 1584000E

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Foster Glacier 782400S 1625000E

Fountain Glacier 774100S 1613800E

Frazier Glacier 770500S 1612500E

Fritter Glacier 770800S 1623500E

Fry Glacier 763800S 1621800E

Gabites Glacier 772054S 1603230E

Garwood Glacier 780100S 1635700E

Gauss Glacier 775800S 1634500E

Gaussiran Glacier 800000S 1591000E

Gawn Ice Piedmont 795800S 1601200E

Gentle Glacier 764600S 1611500E

Geodetic Glacier 774500S 1634800E

Geoid Glacier 774800S 1634700E

Glee Glacier 781600S 1630000E

Glezen Glacier 763200S 1621800E

Glimpse Glacier 781600S 1624600E

Godwit Glacier 773600S 1621200E

Goldman Glacier 774200S 1625100E

Goodspeed Glacier 772900S 1622700E

Gran Glacier 765600S 1611400E

Green Glacier 794300S 1561000E

Griffiths Glacier 771000S 1622000E

Harbour Glacier 770200S 1625400E

Harbour Glacier Tongue 770100S 1625500E

Harp Glacier 773200S 1631400E

Hart Glacier 773000S 1622300E

Haselton Glacier 772115S 1604500E

Haselton Icefall 772100S 1604600E

Hatherton Glacier 795500S 1573500E

Heap Glacier 790300S 1592000E

Hedblom Glacier 763400S 1622400E

Hedley Glacier 774900S 1620700E

Heimdall Glacier 773500S 1615000E

Herbertson Glacier 774200S 1634800E

Hinton Glacier 800300S 1571000E

Hobbs Glacier 775400S 1642400E

Hooker Glacier 780400S 1630600E

Hourihan Glacier 800800S 1584500E
Appendix—Tables 2 and 3 21

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Howard Glacier 774000S 1630500E

Howchin Glacier 781200S 1632200E

Hughes Glacier 774400S 1622700E

Huka Kapo Glacier 772412S 1604300E

Hunt Glacier 765200S 1622500E

Irving Glacier 761300S 1601600E

Jezek Glacier 775900S 1621300E

Joyce Glacier 780100S 1634200E

Judith Glacier 802900S 1584900E

Kamb Glacier 775500S 1623900E

Kehle Glacier 785600S 1601800E

Kempe Glacier 781800S 1625400E

Kennedy Glacier 773900S 1621200E

Kitticarrara Glacier 774300S 1630200E

Koettlitz Glacier 781500S 1641500E

Koettlitz Névé 782700S 1630000E

Kreutz Snowfield 771730S 1611530E

Lacroix Glacier 774000S 1623300E

Landing, The 782200S 1612500E

Lashly Glacier 775700S 1595000E

Lieske Glacier 800500S 1565000E

Lister Glacier 775900S 1630500E

Lobeck Glacier 771315S 1614600E

Loftus Glacier 773300S 1624600E

Lofty Promenade 773100S 1685200E

Lower Jaw Glacier 782200S 1625700E

Lower Staircase 782500S 1614500E

Lugger Glacier 765800S 1605000E

Mackay Glacier 765800S 1620000E

Mackay Glacier Tongue 765800S 1622000E

Marchant Glacier 780600S 1620300E

Marchetti Glacier 771100S 1613300E

Marin Glacier 760400S 1622200E

Marr Glacier 774300S 1624400E

Marston Glacier 765400S 1623000E

Mason Glacier 785300S 1614100E

Matterhorn Glacier 774100S 1622700E

Mawson Glacier 761300S 1620500E

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

McCleary Glacier 793300S 1565000E

McCraw Glacier 800700S 1563500E

McDermott Glacier 782000S 1620400E

McMurdo Ice Shelf 780000S 1663000E

Mercury Glacier 793400S 1571700E

Merrick Glacier 801300S 1585200E

Meserve Glacier 773100S 1621700E

Midship Glacier 765200S 1613000E

Miers Glacier 780500S 1634000E

Miller Glacier 771200S 1620000E

Mime Glacier 773700S 1614500E

Minerva Glacier 793412S 1571500E

Minnehaha Icefalls 770200S 1622400E

Mitchell Glacier 775700S 1630300E

Moa Glacier 774200S 1624600E

Mollweide Glacier 775700S 1634500E

Morning Glacier 782700S 1634800E

Mulock Glacier 790000S 1600000E

Nakai Snowfield 772900S 1613100E

Newall Glacier 773000S 1625000E

New Glacier 770200S 1622400E

Nordenskjöld Ice Tongue 761100S 1624500E

Norris Glacier 774000S 1621200E

Northwind Glacier 764000S 1611800E

Nylen Glacier 774100S 1612900E

Oates Piedmont Glacier 762500S 1623500E

Odell Glacier 764400S 1595500E

Odin Glacier 773500S 1613600E

Orestes Glacier 772700S 1615300E

Overflow Glacier 774700S 1631100E

Overturn Glacier 795400S 1571500E

Packard Glacier 772100S 1621000E

Pakaru Icefalls 773800S 1663900E

Palais Glacier 780200S 1611900E

Pascoe Glacier 764600S 1610100E

Peckham Glacier 802100S 1572500E

Pedalling Ice Field 771500S 1595500E

Petrel Glacier 771400S 1662800E
22 Coastal-Change and Glaciological Map of the Ross Island Area, Antarctica: 1962–2005

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Pipecleaner Glacier 781400S 1625100E

Plane Table Glacier 773400S 1612900E

Plummet Glacier 774700S 1615400E

Potter Glacier 782300S 1621200E

Prebble Icefalls 795400S 1555500E

Priddy Glacier 775600S 1640100E

Prion Glacier 772000S 1663500E

Pyne Glacier 770400S 1621800E

Pūanu Glacier 772330S 1605840E

Quaternary Icefall 771800S 1663000E

Radian Glacier 781300S 1630000E

Ragotzkie Glacier 800200S 1574500E

Ragotzkie Icefall 800300S 1580000E

Ramseier Glacier 803000S 1561800E

Renegar Glacier 782200S 1630800E

Repeater Glacier 772800S 1625100E

Rhone Glacier 774200S 1621400E

Rim Glacier 771300S 1602500E

Ringer Glacier 771500S 1615100E

Rivard Glacier 780400S 1635500E

Robson Glacier 770500S 1621100E

Ross Ice Shelf 813000S 1750000W

Rotunda Glacier 780000S 1613800E

Ruecroft Glacier 781300S 1614000E

Rutgers Glacier 781400S 1615500E

Salient Glacier 780600S 1630500E

Salmon Glacier 775800S 1640500E

Sandy Glacier 772900S 1615700E

Schlatter Glacier 774100S 1612700E

Schultz Glacier 771900S 1622000E

Schutt Glacier 781600S 1613100E

Scrivener Glacier 765700S 1613700E

Scudding Glacier 765400S 1604500E

Scuppers Icefalls 764800S 1613600E

Sefton Glacier 804500S 1565200E

Sennet Glacier 801200S 1584200E

Shark Fin Glacier 782300S 1625500E

Sharpend Glacier 765200S 1605600E

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Shearwater Glacier 771900S 1663100E

Sheathbill Glacier 7718.70S 1663600E

Shell Glacier 771600S 1662500E

Shimmering Icefield 763900S 1594400E

Skelton Glacier 783500S 1613000E

Skelton Icefalls 781400S 1581900E

Skelton Névé 782000S 1600000E

Sollas Glacier 774300S 1623600E

Solomon Glacier 782300S 1623000E

South America Glacier 774900S 1614700E

Spring Glacier 775500S 1630600E

Sprocket Glacier 771200S 1603400E

Stocking Glacier 774200S 1615000E

Stuckless Glacier 781600S 1661200E

Suess Glacier 773800S 1624000E

Sykes Glacier 773500S 1613200E

Taylor Glacier 774400S 1621000E

Tedrow Glacier 775800S 1615000E

Telemeter Glacier 774800S 1601200E

Tern Glacier 771700S 1663200E

Terra Nova Glacier 772700S 1674200E

Terror Glacier 773700S 1680300E

Topside Glacier 764200S 1605700E

Touchdown Glacier 794800S 1581000E

Towle Glacier 763800S 1610500E

Trepidation Glacier 784600S 1622100E

Tripp Ice Tongue 763400S 1624500E

Turnabout Glacier 774600S 1604300E

Twombley Glacier 803500S 1574500E

Upper Jaw Glacier 782100S 1625700E

Upper Staircase 781500S 1610000E

Valhalla Glacier 773400S 1615800E

Vereyken Glacier 782500S 1635700E

Victoria Lower Glacier 771800S 1624000E

Victoria Upper Glacier 771600S 1612500E

Victoria Upper Névé 771600S 1610500E

Von Guerard Glacier 773900S 1632000E

Waddington Glacier 780300S 1612700E
Appendix—Tables 2 and 3 23

Table 3. Inventory of named glaciers and glaciological features 

on the coastal-change and glaciological map of the Ross Island 

area.—Continued

Feature Name Location (latitude, longitude)

Walcott Glacier 781400S 1631500E

Wales Glacier 773700S 1633100E

Walker Glacier 772000S 1603715E

Ward Glacier 781000S 1632700E

Warren Icefall 773300S 1602500E

Weatherwax Glacier 773800S 1633600E

Webb Glacier 771900S 1604500E

Webb Icefall 771600S 1602900E

Wildwind Glacier 765200S 1611000E

Williams Glacier 780600S 1621800E

Willis Glacier 771600S 1620500E

Wilson Piedmont Glacier 771500S 1631000E

Wirdnam Glacier 782500S 1620200E

Wright Lower Glacier 772500S 1630000E

Wright Upper Glacier 773200S 1603500E

Yancey Glacier 801400S 1583000E

Zeller Glacier 805500S 1563000E

Zetland Glacier 780100S 1634900E

Zoller Glacier 775300S 1621800E