Information

Elipsoid, Orthometric, and Geoid heghts relationship

PALSAR RTC DEM Information

Most DEMs are geoid-based and require a correction before they can be used for terrain correction. The DEM included with an ASF RTC product was converted from the orthometric height of the source DEM to ellipsoid height using the ASF MapReady geoid_adjust tool. This tool applies a geoid correction so that the resulting DEM relates to the ellipsoid.

The GeoidEval Utilty is a free online tool that computes the height of the geoid above the WGS84 ellipsoid at a specific location, and will show the amount of correction that was applied to the source DEM used in creating an RTC product.

About the source DEMs used for ALOS PALSAR RTC processing

The quality of an ALOS PALSAR RTC product is directly related to the quality of the digital elevation model (DEM) used in the radiometric terrain correction (RTC) process. The table below summarizes the various DEM sources and the map indicates which DEM was used in a given location.

The continental U.S., Hawaii, and parts of Alaska are covered with 1⁄3 arc-second National Elevation Dataset (NED) at a 10 m resolution. The rest of Alaska above 60 degrees northern latitude was only available at 60 m resolution with 2 arc-second NED data. The best resolution for Canada and Mexico at 30 m was provided by 1 arc-second NED. For the remaining globe, the Shuttle Radar Topography Mission (SRTM) GL1 data at 1 arc-second (30 m) resolution was used. Greenland and Antarctica were mostly covered by ice and glaciers and not suitable for terrain correction. For areas in Eurasia above 60 degrees northern latitude, no suitable DEMs were available.

DEMs used for ALOS PALSAR RTC processing

DEM	Datum	Coverage Area	DEM Resolution	Product Resolution	Resampling Approach
NED13	NAVD88	CONUS, Hawaii, parts of Alaska	~10m (1/3 arc sec)	12.5 m	No resampling
NED13	NAVD88	CONUS, Hawaii, parts of Alaska	~10m (1/3 arc sec)	30 m	Down-sampled DEM to 30-m pixel spacing
SRTMGL1	EGM96	Latitudes between 60 N and 57 S degrees	~30 m (1 arc sec)	12.5 m	Up-sampled 30-m mapping function to 12.5-m mapping function
SRTMGL1	EGM96	Latitudes between 60 N and 57 S degrees	~30 m (1 arc sec)	30 m	No resampling
SRTMUS1	EGM96	CONUS, Hawaii, parts of Alaska	~30 m (1 arc sec)	12.5 m	Up-sampled 30-m mapping function to 12.5-m mapping function
SRTMUS1	EGM96	CONUS, Hawaii, parts of Alaska	~30 m (1 arc sec)	30 m	No resampling
NED1	NAVD88	CONUS, Hawaii, parts of Alaska, Canada, Mexico	~30 m (1 arc sec)	12.5 m	Up-sampled 30-m mapping function to 12.5-m mapping function
NED1	NAVD88	CONUS, Hawaii, parts of Alaska, Canada, Mexico	~30 m (1 arc sec)	30 m	No resampling
NED2	NAVD88	Alaska	~60 m (2 arc sec)	12.5 m	Up-sampled 30-m mapping function to 12.5-m mapping function
NED2	NAVD88	Alaska	~60 m (2 arc sec)	30 m	Up-sampled DEM to 30-m pixel spacing

The DEMs were pre-processed by ASF to a consistent raster format (GeoTIFF) from the original source formats: height (*.hgt), ESRI ArcGrid (*.adf), etc. Many of the NASA-provided DEMs were provided as orthometric heights with EGM96 vertical datum. These were converted to ellipsoid heights using the ASF MapReady geoid_adjust tool. The pixel reference varied from the center (pixel as point) to a corner (pixel as area). The GAMMA software, used to generate the terrain-corrected products, uses pixel as area and adjusts DEM coordinates as needed. Where more than one DEM was available, the best-resolution DEM was used for processing. Complete DEM coverage from a single DEM source was required for processing to proceed.

Image Interpretation

How to View Synthetic Aperture Radar (SAR) Imagery

Most SAR products are delivered in either CEOS or GeoTIFF file formats. These file formats will not display in both Windows and Mac default image viewers. However, you can view GeoTIFFs in a GIS program. In addition, both GeoTIFF and CEOS images can be viewed using free downloadable software from ASF called ASFView. ASFView is included when you download ASF’s MapReady software.

File Format	Dataset	Needed to View
CEOS L1 and L1.5 products	ERS-1, ERS-2, JERS-1, RADARSAT-1, ALOS PALSAR	ASFView (included with ASF MapReady) ASF Data Recipes: How to View and Geocode CEOS Data in ASF MapReady
GeoTIFF products	PALSAR RTC Sentinel-1 – Interferograms	ArcGIS, QGIS ASF Data Recipes: How to View Radiometrically Terrain-Corrected (RTC) Images in ArcGIS and How to View Radiometrically Terrain-Corrected (RTC) Images in QGIS
GeoTIFF products	Terrestrial Ecology, Seasat	ArcGIS, QGIS, ASFView (included with ASF MapReady)

SAR Basics

Basic SAR Concepts and Terminology

Also see: Synthetic Aperture Radar (SAR) and InSAR Guides.

How Does it Work?
A synthetic aperture radar (SAR) is an active sensor that first transmits microwave signals and then receives back the signals that are returned, or backscattered, from the Earth’s surface.

Flight and Directional Terminology
The instrument measures distances between the sensor and the point on the Earth’s surface where the signal is backscattered. This distance is slant range (see illustration), which can be projected on the ground representing the ground range. The flight direction is also referred to as along-track or azimuth direction, and the direction perpendicular to the flight path is the across-track or range direction. The angle between the direction the antenna is pointing and the nadir is the look angle. The angle between the radar beam center and the normal to the local topography is the incidence angle. Both angles are sometimes used synonymously, which is only valid if the InSAR geometry is simplified neglecting the Earth’s curvature and the local topography. Because the look angle of the sensor significantly affects the behavior of backscatter, it is one of the main parameters determining the viewing geometry and the incidence angle of the backscattered signal. Depending on the characteristics of the illuminated terrain, areas of layover and shadow may occur in the imagery.

Wavelength and Effects
The wavelength of the sensor determines the penetration depth of the transmitted signal into the vegetation layer of the terrain surface. The longer the wavelength, the deeper the penetration can be, particularly in forests.

The energy of an X-band sensor is mainly returned at the top layer of the canopies
Most of the L-band signal penetrates through the upper vegetation layer and is returned at the ground surface.
The backscatter behavior of C-band is less predictable. Due to volume scattering effects, the layer of backscattering is less determined and does not correspond directly to a terrain surface — neither the vegetation surface nor the ground surface.

A typical side-looking radar pointing perpendicular to the flight direction. Credit: NASA.

Resolution and Speckle
The spatial resolution of the radar sensor defines the minimum separation between the measurements the sensor is able to discriminate and determines the amount of speckle introduced into the system. Speckle is a scattering phenomenon that arises because the spatial resolution of the sensor is not sufficient to resolve individual scatterers. Speckle can be reproduced if the acquisition conditions are identical, while noise is random in nature. Speckle is removed by multi-looking. The higher the spatial resolution of the sensor, the more objects on the ground can be discriminated. The term spatial resolution is often confused with the pixel size, which is the spacing of the pixels in the azimuth and ground range direction after processing the data.

Custom Processing

ALOS PALSAR The L1.1 (SLC) custom processing service has been discontinued. ASF is in the process of becoming a mirror to the JAXA archive and will soon provide worldwide coverage. If you are currently not able to find L1.1 products using Vertex or the ASF API, keep checking as new products are added to our archive daily.

Sentinel-1 ASF HyP3 (pronounced “hype”) is a user service for processing Synthetic Aperture Radar (SAR) imagery that addresses many common issues for users of SAR data:

Most SAR data require at least some processing to remove distortions before they are analysis-ready
SAR processing requires a lot of computing resources
Software for SAR processing is complicated to use and can be prohibitively expensive
Producing analysis-ready SAR data is hard to learn

HyP3 On-Demand Radiometric Terrain Correction (RTC) and Interferometric SAR (InSAR) processing using GAMMA software are available through the ASF Vertex data search application. This allows you to use the powerful search tools of Vertex and then directly order data for processing without leaving the application. Processing is done in the cloud and results are available to download in less than an hour.

Step-by-step instructions for using the Vertex On-Demand processing services are available in the RTC On Demand! and InSAR On Demand! user guides.

GAMMA RTC and InSAR processing are also available programmatically using the HyP3 API and HyP3 SDK. Detailed information about what these services provide and how to use them can be found in the ASF HyP3 User Guide.

Glacier Power – How do Glaciers Move?

Glaciers Are Solid Rivers

A glacier is a large accumulation of many years of snow, transformed into ice. This solid crystalline material deforms (changes) and moves.
Glaciers, also known as “rivers of ice,” actually flow. Gravity is the cause of glacier motion; the ice slowly flows and deforms (changes) in response to gravity.
A glacier molds itself to the land and also molds the land as it creeps down the valley. Many glaciers slide on their beds, which enables them to move faster.
Rock that falls onto the glacier’s surface is incorporated into the glacier and erodes the bed, forming sediment. The glacier and its load of rock debris flow down-valley.
A glacier discharges snow from its accumulation area in the same way a stream discharges water from its watershed.
Sometimes, in cold climates with a lot of snow, like Alaska, glaciers flow all the way down to sea level. These glaciers carve fjords and make icebergs.
At the glacier’s face, ice which has been melting, fracturing, and has been battered by the sea breaks off as icebergs – a process, called calving, that balances the flow of ice from behind.

Glacier Advance and Retreat

Glaciers advance and retreat. If more snow and ice are added than are lost through melting, calving, or evaporation, glaciers will advance. If less snow and ice are added than are lost, glaciers will retreat.

Accumulation Zone: Where snow is added to the glacier and begins to turn to ice – Input Zone
In this zone, the glacier gains snow and ice.

This is the upper region of the glacier.
Water seeps through accumulated snow and gradually forms horizontal “ice lenses” and vertical “glands.”
Eventually, the whole mass compresses into a deep bed of dense ice.
The ice flows like a conveyor belt driven by gravity and ever mounting snows.

Ablation Zone: Where the glacier loses ice through melting, calving, and evaporation – Output Zone
In this zone, the glacier loses ice.

This is the lower region of the glacier.
Meltwater flows out to the terminus through hidden channels and tunnels.
Oldest ice is the deepest.

Equilibrium Line: An equilibrium line divides the two areas. This spot is like an old-fashioned pair of scales used to weigh gold dust.

If the glacier’s scale, or budget, is balanced with enough new ice added to replace the loss, the glacier is stable, with little advance or retreat.
If the balance is tipped, the glacier shifts and either advances or retreats.

Motion and Movement

Mass Balance: The difference between the amount of material that a glacier accumulates and the amount lost during ablation is called its mass balance. The equilibrium line moves down (1) or up (2) a glacier as the mass balance changes.

Gains more than it loses = positive mass balance
Loses more than it gains = negative mass balance

Ice Flow: Glaciers move by internal deformation (changing due to pressure or stress) and sliding at the base. Also, the ice in the middle of a glacier actually flows faster than the ice along the sides of a glacier as shown by the rocks in this illustration (right).

Glacier Bed: Glaciers move by sliding over bedrock or underlying gravel and rock debris. With the increased pressure in the glacier because of the weight, the individual ice grains slide past one another and the ice moves slowly downhill. The sliding of the glacier over its bed is called the basal slip. Water lubrication is crucial to either process.

Revealed by Satellite Radar

These images allow glaciologists to study in very fine detail the way in which glacier ice flows downhill. An “interferogram” is an image made from the comparison of two radar satellite scenes of a glacier. The cycle, or repeating, color patterns represent an overlaying of information about surface elevation (like topographic maps) with information about how fast the surface of the glacier is moving.

The glaciers in the images are part of the Bagley Icefield in Southcentral Alaska. On the mountains (which are stationary), the color bands represent increasing elevation. On the glacier surface the color bands primarily represent surface speed.

In these images the color bands are like a series of parallel moving sidewalks, each moving slightly faster than its neighbor as one traverses from the edge of the glacier towards the center, so that the ice in the middle is moving the fastest.

Moraine: Moraines are mounds, ridges, or other distinct accumulations of unsorted, unlayered mixtures of clay, silt, sand, gravel, and boulders. There are many types of moraines:

Terminal or toehold – The advancing ice scrapes and grinds the bedrock boulders and gravel beneath it and pushes ahead of itself a ridge or terminal moraine of rock and earth. A terminal moraine helps to anchor the glacier’s ice.
Lateral – their rock material comes from the valley walls.
Medial – When two lateral moraines combine, or a tributary glacier joins the main flow, they form a single medial moraine, which extends as a long, dark stripe down the middle of the glacier towards the snout. When medial moraines come close to one another near the terminus, a glacier may look multicolored or striped. Medial moraines can create interesting swirls and loops.
Ablation – an accumulation of melted-out rocks (sometimes just sparse collections of glacial till).
End and Push – created near the margin of a glacier, at the terminus.
Ground and Dump – glaciers often dump out their supply of rocks as they retreat.

Terminus: The terminus is the lowest end of a glacier. Also called the snout, toe, or leading edge. Near the terminus, the glacier’s surface thins and stretches and breaks into a mosaic of crevasses. Below, the terminus of Hubbard Glacier in Alaska is shown as a large chunk of it is breaking off (also called, “calving”).

Meltwater flows through hidden channels and tunnels, reaching the base of the ice to lubricate its flow, and pours from under its face in a silt-laden cloud.

Nunatak is an Inuit term for an island of bedrock or mountain projecting above the surface of an ice sheet, highland icefield, or mountain glacier. The glacier flow has gone around the bedrock, leaving behind this distinct geologic feature.

Hubbard Glacier, Alaska. Photo by Alean.

Glacier flour. Photo by Dr. Bruce Molnia, Alaska Geographic Society.

Nunatak. Photo by Alaska Geographic Society.

Scientists use stakes to measure glacier movement. In the picture to the right below, the glacial stream velocity is being measured by a scientist.

Glaciers advance and retreat in response to changes in climate. As long as a glacier accumulates more snow and ice than it melts or calves, it will advance.

How do Glaciers Move?

Vocabulary Plus!

accumulation zone

debris

watershed

discharge

ablation zone

equilibrium line

mass balance

deformation

calving

crampons

crevasse probe

tributary

moraine

terminal

lateral

medial

glacier bed

basal slip

terminus

meltwater

rope

gravity

Review Questions

(some of the answers may come from the vocabulary list)

What causes the glacier to be in motion?
True or False: Glaciers slide on their beds and this enables them to move faster.
True or False: Glaciers can’t flow down to sea level or carve fjords.
What is the zone where a glacier gains snow and ice?
What is the zone where a glacier loses ice through melting and calving?
What is the difference between the amount of material that a glacier accumulates and the amount it loses during ablation?
If the glacier gains more than it loses, will the glacier have a positive or negative mass balance?
True or False: The snout is another name for the terminus on a glacier.
Name one type of moraine.

Brain Challenge!

When climbing a glacier, if you could only bring one other thing with you besides warm clothes, boots, and a camera, what would you bring?

Exercise: Connect the Words with Definitions
Draw lines to connect the words to their definitions

Ablation zone

Accumulation zone

Calving

Moraine

Equilibrium line

Terminus

lowest end of a glacier

soil and rock debris

equal melting/adding

losing snow

adding snow

ice breaking off

Project: More Silly Putty Cigars

Roll some Silly Putty into a cigar shape to make it look like a glacier. Then grab the ends and pull it slowly apart. See it sag and still stay as one piece. This is like ice. When ice moves slowly, it flows and deforms.

(Courtesy Glaciers of North America, By S. Ferguson)

Firn line marked on Vedretta di Fellario Orientale Glacier in the Italian Alps. The firn line is the zone that separates bare ice from snow at the end of the ablation season. Photo by Alean.

Glacier Power – How do Glaciers Form?

From Snowflakes to Rivers of Ice

Glaciers are massive and incredibly powerful, but they begin with small snowflakes. Imagine how many snowflakes make a glacier as snow gradually changes into glacier ice.

The firn line on a glacier is the zone that separates bare ice from snow at the end of the ablation season.

Recipe for a Glacier

Snowfall on a glacier is the first step in the formation of glacier ice.
As snow builds up, snowflakes are packed into grains.
The weight of the overlying snow causes the grains below to become coarser and larger. (Fresh snow is about 90 percent air.)
Melted snow quickly refreezes forming ice. How the snow changes and how much time it takes to develop into glacier ice depends on the temperature.

In an area where there is more snowfall than summer snow melt, perennial snow patches appear in the mountains and remain at the end of summer. Glaciers can form in areas where summer temperatures are too low for all of the snow to melt.

When the weight of the ice and snow (thickening snowfield) becomes great enough, they begin to move (flow down-slope). When signs of flow appear in a perennial snow patch, a glacier has begun! No longer only a mass of ice and snow, it is a glacier!

Folia/Foliations are individual layers or bands of ice crystals produced during the metamorphic process and compression that changes snow to glacier ice. The layers have distinctive crystal sizes and usually alternate between bubbly and clear ice or between fine-grained and coarse-grained ice. Photo by Hambrey.

Staging area on a glacier's névé, the area covered with snow throughout the year. The term also refers to the accumulation area at the upper end of a glacier. Glaciologists land their planes in this area, as it is relatively safe from crevassing.
Photo by James Roush. — Staging area on a glacier's névé, the area covered with snow throughout the year. The term also refers to the accumulation area at the upper end of a glacier. Glaciologists land their planes in this area, as it is relatively safe from crevassing. Photo by James Roush.

Firn is wetted snow that has survived one summer without being transformed to ice. It is in the metamorphic process of snow-becoming-ice. Eventually, firn changes into solid glacier ice.
Firn takes about a year to form. (In colder parts of the world, this could take as long as 100 years.)
Firn becomes glacier ice when the interconnecting air passages between the grains are sealed off. In glacier ice, air is present only as bubbles. Ice may become denser by more compression of the bubbles.

Remember, the scanning electron micrographs of the firn crystals and the snowflake shown in What is a Glacier? Here again, you can see the great difference between snow and firn. There is also a great difference between firn crystals and glacier ice crystals.

How do Glaciers Form?

Vocabulary

firn
perennial
firn line
metamorphic
compression
snowflake
gravity

Review Questions
(Some of the answers may come from the vocabulary list.)

The formation of a huge glacier begins with a single, small _____________?
What types of summer temperatures need to occur for a glacier to form?
How does over-lying weight affect the snow?
What is wetted snow that has survived one summer without being transformed into glacier ice?
How long does it take for firn to form?
When does firn become glacial ice?
What is the line that separates bare ice from snow at the end of the ablation season?
What is the difference between a perennial snow patch and a glacier?
What causes a glacier to move downhill?

Brain Challenge!
What would Alaska look like if all of the glaciers melted?

Exercise: Circle the Facts
Circle all the statements that are true about each word is given (more than one statement may be true).

Firn:

A. is wet snow that has survived one summer without being completely turned into ice

B. are plants your cat likes to eat

C. takes a year to form

D. becomes glacier ice when it is more compressed

E. is what you call snow when it’s freshly fallen on the glacier

Snowflake(s):

A. change to firn

B. is the name of your pet rattlesnake

C. is the first step in the formation of glacier ice

D. is a six-sided crystal

E. can’t form glacier ice

Snow on a glacier:

A. is only used for snowball fights

B. builds up on a glacier in the accumulation zone

C. causes the grains of snow beneath it to enlarge

D. will melt instantly because the glacier is so hot

E. will feed all the ice worms

Project: Firn Structure

You’ll need:

snow or ice shavings from ice cubes or freezer frost
very cold water (close to freezing)
a small container that you can seal
a larger container

Mix the ice in your small container with enough water to make a slushy snow. Seal the container. Next, make an ice bath with a mixture of half water and half ice and sink your sealed container into the bath. If you’re able, put the whole experiment into a refrigerator.
After 24 hours, remove the sealed container and drain all the water. Use some tissue to pat dry the snow.
Reseal the container and put it back in the ice bath for a few hours.
When this is done, pull the sealed container out and look at the remaining ice with a magnifying lens of at least 5x magnification. You should see clusters of rounded ice particles, very similar to the structure of firn.

(Courtesy of Glaciers of North America, By S. Ferguson)

The Start of a Moulin. Photo by James Roush.

Glacier Power – How are Glaciers Strange?

Glacier Voices

Glaciers are giants that seem to come to life with strange voices, mysterious powers and unusual life forms. These voices can be of a substantial volume. The sounds that they produce can be as comforting as your breakfast cereal or as terrifying as a creature from Jurassic Park.

Ice Sizzles can sound like Rice Krispies^TM or Pepsi Cola^TM
Ice Quakes are the first indication that a crevasse is forming but they don’t sound like the low rumbling of earthquakes. Fractures that cause ice quakes make a hissing or traveling cracking sound which sometimes comes from within the glacier, even though no crack is visible on the surface.
Moulins, which are holes in the glacier, allow for waterflow and make loud roaring sounds.

The End of the Same Moulin. Photo by James Roush.

Glacier Life

As glaciers shift and change the face of the earth with their giant hands, they delicately support some of the tiniest creatures alive. Glaciers create unusual environments sensitive to the animal kingdom’s need for existence.

Glacier fleas are small black wingless springtail bugs that live in firn on glaciers.
Ice worms feed on algae and pollen, as they thrive in the cold temperatures of glaciers.

Ice worms compared to a penny. Photo by Harvey Bowers.

Scanning Electron Micrograph of an actual ice worm. W.P. Wergin & E.F. Erbe, ARS, U.S.D.A.

Fossils

Fossils may be trapped in glaciers for thousands of years.

Glacier Force

When the Hubbard Glacier surged in 1986, a tongue of ice blocked the mouth of Russel Fjord creating a very large lake. The first signs of a surge are thickening of ice in the upper part of a glacier and then the appearance of lots of crevasses. During a surge, a glacier can flow more than 100 times faster than it normally flows.

Jokulhlaups (or “outburst floods”) can bring a sudden end to the surge of a glacier by releasing stored subglacial water. This water, on which the glacier was “walking,” enables the glacier to slide rapidly on its bed. Jokulhlaups are sudden glacial outburst floods of water that can be catastrophic. During the summer of 1994 the surge of Bering Glacier was ended by a Jokulhlaup or outburst flood with a sudden release of stored water from within the glacier. The force of the Jokulhlaup caused large segments of ice to calve. The enormous splashes and force represented were awesome.

The force of the pent-up water bursting forth is amazing. Huge boulders of ice are rolled and swallowed easily.

Strange Glacier Phenomena

Vocabulary Plus!

ice sizzles
ice quakes
moulins
glacier fleas
ice worms
fossils
Jokulhlaups
algae
pollen

Review Questions
(some of the answers may come from the
vocabulary list)

Can glaciers make sounds?
What are the small black wingless springtail bugs that live in firn on glaciers?
What do ice worms eat?
There is an image of a fossil in glacial till in this section. What is the fossil?
What are sudden glacial outburst floods of water that can be catastrophic?
Do ice quakes sound like earthquakes (a rumbling sound) or do they make a hissing and crackling sound?
Are moulins holes in a glacier or the steel spikes you put on your boots to hike on a glacier?

Brain Challenge!
Would you ever want to be an ice worm?
Why or why not?

Exercise: Crossword Puzzle
Choose 5 out of the 7 words given for the crossword puzzle.

Possible words:
moulins
ice worms
Jokulhlaups
fossils
ice sizzle
glacier
ablation

Down

outburst flood
sounds like crispy rice cereal

Across

holes in a glacier allowing water to flow
things that can be trapped in a glacier for
thousands of years
living in a glacier

Project: Hair Spray the Snow
Hey kids! If there’s snow outside, here’s a cool project to try! Get a clear piece of plastic that has been chilled outside. Grab a bottle of hairspray. Go outside and catch a few snowflakes. Spray the hairspray to preserve the snowflakes. Look at the snowflakes with a hand lens. Draw a picture of what you see! NEAT!

(Courtesy of Glaciers of North America, By S. Ferguson)

Glacier Power – How Dangerous are Glaciers?

Glaciers Have Their Own Warning Signs

Glaciers can be dangerous in many ways. However, as long as you keep safety in mind, visiting a glacier can be a wonderful experience.

Walking too close to a glacier can be hazardous! Often the ice will form cliffs at the terminus (the end of the glacier) or at the margins (the sides). Sometimes the ice makes towers called seracs.

Be Careful!

These cliffs and ice towers are unstable and can fall. Glaciers are always moving slowly, even though you usually can’t see them move. The movement causes stress. The stress causes cracking, which causes blocks of ice to break off and fall. Sometimes an entire serac or section of the ice front can collapse. People standing too close could be killed by falling ice.

Crevasses are dangerous

Sometimes crevasses are not visible because they are covered by surface snow. This can happen during winter snowstorms when wind causes the drifting snow to build out from the upwind side of the crevasse. Mechanical hardening of the snow, caused by wind drifting, enables the snowflakes or grains to stick together as the snow bridges out toward the downwind side of the crevasse. Finally, the crevasse is completely covered. In this way, large crevasses can be entirely hidden beneath a thin layer of snow.

Sometimes a crevasse stretching for a long way across a glacier will have a single snow bridge, which may sag into the crevasse under its own weight. Snow bridges can be strong enough to support the weight of a person, but crossing them is risky. People, snow machines (no matter how fast they are going) and, in Antarctica, even large pieces of machinery have been known to fall into covered or bridged crevasses.

Living Near Glaciers Can Be Dangerous!

In the village of Randa in Switzerland, parts of the hanging glacier below the summit have broken and fallen. Ice avalanches in the winter can cause enormous masses of snow to move and the subsequent avalanches have reached as far as the tiny village in the foreground.

Safety

A person should never walk on a glacier alone. The risk of slipping on the ice and sliding into an open crevasse, or of breaking through and falling into a hidden crevasse is too great. It would be very hard, or impossible, for a single person to get out of a crevasse without companions who have a rope and other equipment. This is especially true if the person is injured in the fall.

Glaciologists and mountaineers or glacier travelers are all extremely wary of crevasses. Before making camp on a glacier, they will use crevasse probes (a 10 meter long metal rod) to detect hidden crevasses. They also practice methods of rescuing a companion who has fallen into a crevasse, and of getting themselves out. For safety, they tie themselves together in groups of two or three using a rope about 45 meters (150 ft) long. They carry ice axes to stop themselves from sliding. If they are pulled down by one person falling into a crevasse, the ice axes help stop the fall. To keep from slipping on ice, they wear crampons, which are steel spikes attached to the bottoms of their boots.

The correct way to travel on a glacier:

Travel in a team
Team members may be roped together
Have an experienced glacier traveler with your team
Use proper equipment

Special Equipment:

Ice Axes
Ropes
Crampons
Crevasse Probes

Proper Clothing:

Boots, waterproof and warm
High tech materials for warm clothing, or dress in layers of clothing
Don’t forget your handy duct tape!

Glacier Danger and Safety

Vocabulary Plus!

seracs
snow bridges
crampons
crevasse
stress
ice axe
crevasse probe

Review Questions
(some of the answers may come from the vocabulary list)

What is a tower of ice surrounded on all sides by crevasses?
What causes a block of ice to break off and fall?
What do snow bridges cover on a glacier?
Does wind drifting cause mechanical hardening in the snow?
Should you walk over a snow bridge?
What do glacier travelers wear on their boots so they don’t slide on the ice?
Name two correct ways to travel on a glacier.
Name a piece of proper clothing to wear when traveling on glaciers.
If they go fast enough, snow machines can cross a snow bridge safely. True or False?

Brain Challenge!

What one thing would you like to do on a glacier?

Exercise: Dress Your Friend for His/Her Hiking Adventure

Your friend, Pat, is going to hike on Bering Glacier. Choose the right clothing and gear for his/her journey.
Please draw in the correct clothing.

Here’s a list of possible items. Which ones are right?

coloring book

crampons

video games

jacket

rope

gloves

bathing suit

hockey stick

blow dryer

bicycle

experienced traveler

boots

sandals

football

ice skates

camera

Project: Double Fisherman’s Knot

When groups of climbers climb across glaciers and up mountains, they often will connect to each other with ropes. This can save lives in the case of an avalanche. The trick is to make sure one person at the end of a rope is standing in a safe spot, out of an avalanches’ way, while the person at the other end of the rope crosses the dangerous slope. This way, it reduces the chance that the exposed climber will be swept away by the force of the avalanche.

A knot that’s often used to connect two ropes is called the double fisherman’s knot. Tying knots may seem tricky at first, but it’s fun! Let’s try this knot:

You’ll need two pieces of rope, about one to one-and-a-half yards long each.

Citation Policy for Data and Imagery Accessed Through ASF

Instructions for specific datasets

Whenever you publish data processed or archived at ASF or ASF DAAC, cite ASF or ASF DAAC as the data source, following the guidelines below. Examples include but are not limited to papers, presentations, websites, videos, and books. When you discuss with news organizations your use of data processed or archived at ASF or ASF DAAC, please cite ASF or ASF DAAC as well as the data source. In general, cite the following elements:

Name of dataset
Source of original data (requirements may vary depending on source; see links below)
Year of data acquisition
“Processed by ASF” if applicable or “Processed by ASF DAAC” if applicable
“Retrieved from ASF [day month year of data access]” or “Retrieved from ASF DAAC” if the data are ASF DAAC data
DOI when available (some datasets have their own DOIs)

Crediting Imagery

Include credit with each image shown in publications such as journal papers, articles, posters, and websites. See links below for specific formats and examples for datasets with their own requirements.

The general guidelines are to credit the source organization with a copyright symbol and cite the year of data acquisition. For derivative images, cite the creator, date of image creation, source organization, and date of data acquisition.

About ASF DAAC datasets: ASF DAAC datasets are provided through the NASA Earth Science Data and Information System (ESDIS) project. ASF DAAC is one of the Earth Observing System Data and Information System (EOSDIS) Distributed Active Archive Centers (DAACs), part of the ESDIS project. NASA data are not copyrighted; however, when you publish NASA data or results derived therefrom, NASA requests that you include an acknowledgment within the text of the publication and reference list. See the examples below.

Please note that some datasets, particularly those from foreign space agencies, have special citation requirements.

Links to Specific Citation Formats and Examples

ASF DAAC SAR Datasets			Other Data
AIRSAR	ALOS PALSAR	SMAP	GISMO
ERS-1	RADARSAT-1	Terrestrial Ecology	Glacier Speed
ERS-2	Sea Ice MEaSUREs	UAVSAR	Polar Year 07-08
InSAR	Seasat	Wetlands MEaSUREs	RAMP
JERS-1	Sentinel-1

Using ASF Web Information

Some images at this website are explicitly restricted from reuse without the author’s permission. Where images are not marked, you may reuse them but must include any copyright associated with the image. Whenever you use any materials from this website, please also acknowledge ASF as follows: “Information [and images] on [SUBJECT] obtained from https://asf.alaska.edu, Alaska Satellite Facility, UAF, [Month, Year].”

Please send reprints and two copies of any work citing ASF data to uso@asf.alaska.edu, with “New ASF Citation” in the subject line or to

Alaska Satellite Facility User Services
2156 Koyukuk Dr
Fairbanks, AK 99775

Questions?

If you have any questions about using ASF data or information, please contact us.

Root Glacier. Photo by the Alaska Geographic Society.

Glacier Power – What is a Glacier?

A Glacier Begins with Small Snowflakes

Glaciers are massive and incredibly powerful but they begin with small snowflakes.

Each lacy, delicate crystal flake is unlike any other; imagine how many it takes to make a glacier as snow gradually changes into glacier ice.

What is a Glacier? A glacier is a huge mass of many years of snow, ice, rock, sediment, and water. It originates on land and moves down slope under the influence of its own weight and gravity.

Each glacier is different in its own special way and each glacier has a different surrounding environment.

Moraines at Glacier Bay. Photo by Stephen J. Kraseman.

Ice Sheets, Shelves, and Caps

Ice Sheets

Found in Antarctica and Greenland.
Large masses of ice which cover more than 50,000 square kilometers!
Some ice sheets that flow into the sea have ice streams.

Ice Shelves are slabs of glacier ice which float on the sea. Glaciers that discharge into the sea from higher ground become detached from the bed and float, spreading out to cover large bays.

Ice Caps

They are smaller versions of Ice Sheets which cover less than 50,000 square kilometers. A large ice cap could cover an area as large as the entire Seward Peninsula on Alaska’s west coast!
Ice accumulates on a high area in the middle of an ice cap and spills down on all sides.

Mountain Glaciers

Cirques

Are bowls or basins carved out of a mountain.
Are very short in relation to their width.

Valley Glaciers

Are found in high altitudes.
May flow downwards from cirques, ice caps, highland ice fields, or ice sheets.
Are shaped like long tongues of ice.
Bering and Hubbard Glaciers are valley glaciers and are the longest in the Americas (200 and 150 kilometers long).

Tidewater Glaciers

Are valley glaciers that enter the sea. At the water, they either remain grounded or float.

Piedmont Glaciers

Formed where mountain valleys open into larger valleys or onto plains.
Valley glaciers that spread out into wide lobes.

Ice Aprons or Hanging Glaciers

Form where mountain slopes seem almost too steep to hold any snow
Often make avalanches.

Hubbard Glacier is a Tidewater Glacier. Photo by Sharp.

Small piedmont bulb of ice near Dobbin Bay on
Ellesmere Island, Canadian Arctic. Photo by Sharp. — Small piedmont bulb of ice near Dobbin Bay on Ellesmere Island, Canadian Arctic. Photo by Sharp.

Synthetic Aperture Radar (SAR) satellite image of Malaspina Glacier, Alaska. SAR Image © ESA 1992.

Types of Glaciers (By Temperature)

Warm (or Temperate) Glaciers

Ice is at the melting point throughout.
Meltwater is abundant in summer and continues to flow throughout the winter.
A well-developed drainage network exists, including moulins, ice lenses, and water pockets.
Form in most mountain regions outside the Arctic and Antarctic.
The glacier is eroded.

Cold Glaciers

Most of the ice is at temperatures below freezing.
Are frozen to the bed and erode very little.
Are found in the polar and sub-polar regions (sub-polar glaciers melt at the surface in summer).

Beginnings

Remember, even the largest glacier begins with a small snowflake! Here is an example of a snowflake crystal. It has been greatly magnified and is a scanning electron micrograph of the snow crystal. Next to it is what happens to the snow crystals when they begin the process of compression and are on their way to becoming glacier ice. These other crystals are also scanning electron micrographs of firn crystals.

What is a Glacier?

Vocabulary Plus!

glacier
ice sheet
ice cap
cirque
valley glacier
tidewater glacier
piedmont glacier
hanging glacier
warm (temperate) glacier
cold glacier
Antarctica
Greenland
Highland Ice Field
Synthetic Aperture Radar

Review Questions
(some of the answers may come from the vocabulary list)

How does the glacier move down slope?
Are all glaciers the same?
Where are the world’s largest ice sheets found?
Do ice shelves float?
Which are bigger, ice shelves or ice caps?
From what sources might you see a valley glacier flowing?
What does SAR stand for?
In what season is meltwater abundant, summer or winter?
Do cold glaciers erode a lot?

Brain Challenge!
When rivers freeze, do they turn into glaciers?

Project: Snowball Melt and Freeze
Let’s see how a glacier is made!
You’ll need:

A small mound of snow from outside (if available)
OR 10 to 12 ice cubes, finely crushed
OR scraped ice from the sides of your freezer at home
A small handful of dirt
A few pebbles

Now, mix the snow with the dirt and pebbles, then form into a tight ball. Put in the freezer. Once the ball’s frozen hard, bring it back out into room temperature. Let it rest until it just starts to melt. Pack tightly again with your hands. Return to freezer, and remove again once it’s hard.

Repeat the steps two or three times. Notice that each time you pack the snowball, it gets tighter and more compact. That means there are fewer air bubbles in the ice because of the pressure applied by your hands. This is similar to how a glacier is made. The weight of snow and ice on a glacier presses the snow tight over time, removing many air bubbles.

(Courtesy of Glaciers of North America, by S. Ferguson)

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Alaska Satellite Facility: Making remote-sensing data accessible.

The Alaska Satellite Facility

About the source DEMs used for ALOS PALSAR RTC processing

DEMs used for ALOS PALSAR RTC processing

How to View Synthetic Aperture Radar (SAR) Imagery

Basic SAR Concepts and Terminology

Glaciers Are Solid Rivers

Glacier Advance and Retreat

Motion and Movement

Revealed by Satellite Radar

How do Glaciers Move?

From Snowflakes to Rivers of Ice

All About Firn

How do Glaciers Form?

Glacier Voices

Glacier Life

Fossils

Glacier Force

Strange Glacier Phenomena

Glaciers Have Their Own Warning Signs

Safety

Glacier Danger and Safety

Instructions for specific datasets

Crediting Imagery

Links to Specific Citation Formats and Examples

Using ASF Web Information

A Glacier Begins with Small Snowflakes

Types of Glaciers (By Where They Are)

Ice Sheets, Shelves, and Caps

Mountain Glaciers

Types of Glaciers (By Temperature)

Beginnings

What is a Glacier?

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