Permeability (electromagnetism)

From Wikipedia, the free encyclopedia
https://en.wikipedia.org/wiki/Permeability_(electromagnetism)

In electromagnetism, permeability is the measure of magnetization produced in a material in response to an applied magnetic field. Permeability is typically represented by the (italicized) Greek letter μ. It is the ratio of the magnetic induction ${\displaystyle B}$ to the magnetizing field ${\displaystyle H}$ as a function of the field ${\displaystyle H}$ in a material. The term was coined by William Thomson, 1st Baron Kelvin in 1872, and used alongside permittivity by Oliver Heaviside in 1885. The reciprocal of permeability is magnetic reluctivity.

In SI units, permeability is measured in henries per meter (H/m), or equivalently in newtons per ampere squared (N/A²). The permeability constant μ₀, also known as the magnetic constant or the permeability of free space, is the proportionality between magnetic induction and magnetizing force when forming a magnetic field in a classical vacuum.

A closely related property of materials is magnetic susceptibility, which is a dimensionless proportionality factor that indicates the degree of magnetization of a material in response to an applied magnetic field.

Explanation

In the macroscopic formulation of electromagnetism, there appear two different kinds of magnetic field:

• the magnetizing field H which is generated around electric currents and displacement currents, and also emanates from the poles of magnets. The SI units of H are amperes/meter.
• the magnetic flux density B which acts back on the electrical domain, by curving the motion of charges and causing electromagnetic induction. The SI units of B are volt-seconds/square meter (teslas).

The concept of permeability arises since in many materials (and in vacuum), there is a simple relationship between H and B at any location or time, in that the two fields are precisely proportional to each other:

${\displaystyle \mathbf{B}=\mu \mathbf{H}}$,

where the proportionality factor μ is the permeability, which depends on the material. The permeability of vacuum (also known as permeability of free space) is a physical constant, denoted μ₀. The SI units of μ are volt-seconds/ampere-meter, equivalently henry/meter. Typically μ would be a scalar, but for an anisotropic material, μ could be a second rank tensor.

However, inside strong magnetic materials (such as iron, or permanent magnets), there is typically no simple relationship between H and B. The concept of permeability is then nonsensical or at least only applicable to special cases such as unsaturated magnetic cores. Not only do these materials have nonlinear magnetic behaviour, but often there is significant magnetic hysteresis, so there is not even a single-valued functional relationship between B and H. However, considering starting at a given value of B and H and slightly changing the fields, it is still possible to define an incremental permeability as:

${\displaystyle \mathrm{\Delta }\mathbf{B}=\mu \mathrm{\Delta }\mathbf{H}}$.

assuming B and H are parallel.

In the microscopic formulation of electromagnetism, where there is no concept of an H field, the vacuum permeability μ₀ appears directly (in the SI Maxwell's equations) as a factor that relates total electric currents and time-varying electric fields to the B field they generate. In order to represent the magnetic response of a linear material with permeability μ, this instead appears as a magnetization M that arises in response to the B field: ${\displaystyle \mathbf{M}=\left({\mu }_0^{-1}-{\mu }^{-1}\right)\mathbf{B}}$. The magnetization in turn is a contribution to the total electric current—the magnetization current.

Relative permeability and magnetic susceptibility

Relative permeability, denoted by the symbol ${\displaystyle {\mu }_{\mathrm{r}}}$, is the ratio of the permeability of a specific medium to the permeability of free space μ₀:

${\displaystyle {\mu }_{\mathrm{r}}=\frac{\mu }{{\mu }_0},}$

where ${\displaystyle {\mu }_0\approx }$ 4π × 10⁻⁷ H/m is the magnetic permeability of free space. In terms of relative permeability, the magnetic susceptibility is

${\displaystyle {\chi }_m={\mu }_r-1.}$

The number χ_m is a dimensionless quantity, sometimes called volumetric or bulk susceptibility, to distinguish it from χ_p (magnetic mass or specific susceptibility) and χ_M (molar or molar mass susceptibility).

Diamagnetism

Main article: Diamagnetism

Diamagnetism is the property of an object which causes it to create a magnetic field in opposition of an externally applied magnetic field, thus causing a repulsive effect. Specifically, an external magnetic field alters the orbital velocity of electrons around their atom's nuclei, thus changing the magnetic dipole moment in the direction opposing the external field. Diamagnets are materials with a magnetic permeability less than μ₀ (a relative permeability less than 1).

Consequently, diamagnetism is a form of magnetism that a substance exhibits only in the presence of an externally applied magnetic field. It is generally a quite weak effect in most materials, although superconductors exhibit a strong effect.

Paramagnetism

Main article: Paramagnetism

Paramagnetism is a form of magnetism which occurs only in the presence of an externally applied magnetic field. Paramagnetic materials are attracted to magnetic fields, hence have a relative magnetic permeability greater than one (or, equivalently, a positive magnetic susceptibility).

The magnetic moment induced by the applied field is linear in the field strength, and it is rather weak. It typically requires a sensitive analytical balance to detect the effect. Unlike ferromagnets, paramagnets do not retain any magnetization in the absence of an externally applied magnetic field, because thermal motion causes the spins to become randomly oriented without it. Thus the total magnetization will drop to zero when the applied field is removed. Even in the presence of the field, there is only a small induced magnetization because only a small fraction of the spins will be oriented by the field. This fraction is proportional to the field strength and this explains the linear dependency. The attraction experienced by ferromagnets is non-linear and much stronger so that it is easily observed, for instance, in magnets on one's refrigerator.

Gyromagnetism

For gyromagnetic media (see Faraday rotation) the magnetic permeability response to an alternating electromagnetic field in the microwave frequency domain is treated as a non-diagonal tensor expressed by:

${\displaystyle \begin{array}{rl}\mathbf{B}(\omega )& =\left|\begin{array}{ccc}{\mu }_1& -i{\mu }_2& 0\\ i{\mu }_2& {\mu }_1& 0\\ 0& 0& {\mu }_z\end{array}\right|\mathbf{H}(\omega )\end{array}}$

Values for some common materials

The following table should be used with caution as the permeability of ferromagnetic materials varies greatly with field strength. For example, 4% Si steel has an initial relative permeability (at or near 0 T) of 2,000 and a maximum of 35,000 and, indeed, the relative permeability of any material at a sufficiently high field strength trends toward 1 (at magnetic saturation).

Magnetic susceptibility and permeability data for selected materials

Medium	Susceptibility, volumetric, SI, χm	Relative permeability, max., μ/μ0	Permeability, μ (H/m)	Magnetic field	Frequency, max.
Vacuum	0	1, exactly	1.25663706212 × 10−6 (μ0)
Metglas 2714A (annealed)		1000000	1.26×100	At 0.5 T	100 kHz
Iron (99.95% pure Fe annealed in H)		200000	2.5×10−1
Permalloy		100000	1.25×10−1	At 0.002 T
NANOPERM®		80000	1.0×10−1	At 0.5 T	10 kHz
Mu-metal		50000	6.3×10−2
Mu-metal		20000	2.5×10−2	At 0.002 T
Cobalt-iron (high permeability strip material)		18000	2.3×10−2
Iron (99.8% pure)		5000	6.3×10−3
Electrical steel		4000	5.0×10−3	At 0.002 T
Ferritic stainless steel (annealed)		1000 – 1800	1.26×10−3 – 2.26×10−3
Martensitic stainless steel (annealed)		750 – 950	9.42×10−4 – 1.19×10−3
Ferrite (manganese zinc)		350 – 20 000	4.4×10−4 – 2.51×10−2	At 0.25 mT	approx. 100 Hz – 4 MHz
Ferrite (nickel zinc)		10 – 2300	1.26×10−5 – 2.89×10−3	At ≤ 0.25 mT	approx. 1 kHz – 400 MHz
Ferrite (magnesium manganese zinc)		350 – 500	4.4×10−4 – 6.28×10−4	At 0.25 mT
Ferrite (cobalt nickel zinc)		40 – 125	5.03×10−5 – 1.57×10−4	At 0.001 T	approx. 2 MHz – 150 MHz
Mo-Fe-Ni powder compound (molypermalloy powder, MPP)		14 – 550	1.76×10−5 – 6.91×10−4		approx. 50 Hz – 3 MHz
Nickel iron powder compound		14 – 160	1.76×10−5 – 2.01×10−4	At 0.001 T	approx. 50 Hz – 2 MHz
Al-Si-Fe powder compound (Sendust)		14 – 160	1.76×10−5 – 2.01×10−4		approx. 50 Hz – 5 MHz
Iron powder compound		14 – 100	1.76×10−5 – 1.26×10−4	At 0.001 T	approx. 50 Hz – 220 MHz
Silicon iron powder compound		19 – 90	2.39×10−5 – 1.13×10−4		approx. 50 Hz – 40 MHz
Carbonyl iron powder compound		4 – 35	5.03×10−6 – 4.4×10−5	At 0.001 T	approx. 20 kHz – 500 MHz
Carbon steel		100	1.26×10−4	At 0.002 T
Nickel		100 – 600	1.26×10−4 – 7.54×10−4	At 0.002 T
Martensitic stainless steel (hardened)		40 – 95	5.0×10−5 – 1.2×10−4
Austenitic stainless steel		1.003 – 1.05	1.260×10−6 – 8.8×10−6
Neodymium magnet		1.05	1.32×10−6
Platinum		1.000265	1.256970×10−6
Aluminum	2.22×10−5	1.000022	1.256665×10−6
Wood		1.00000043	1.25663760×10−6
Air		1.00000037	1.25663753×10−6
Concrete (dry)		1
Hydrogen	−2.2×10−9	1.0000000	1.2566371×10−6
Teflon		1.0000	1.2567×10−6
Sapphire	−2.1×10−7	0.99999976	1.2566368×10−6
Copper	−6.4×10−6 or −9.2×10−6	0.999994	1.256629×10−6
Water	−8.0×10−6	0.999992	1.256627×10−6
Bismuth	−1.66×10−4	0.999834	1.25643×10−6
Pyrolytic carbon		0.9996	1.256×10−6
Superconductors	−1	0	0

Magnetisation curve for ferromagnets (and ferrimagnets) and corresponding permeability

A good magnetic core material must have high permeability.

For passive magnetic levitation a relative permeability below 1 is needed (corresponding to a negative susceptibility).

Permeability varies with a magnetic field. Values shown above are approximate and valid only at the magnetic fields shown. They are given for a zero frequency; in practice, the permeability is generally a function of the frequency. When the frequency is considered, the permeability can be complex, corresponding to the in-phase and out of phase response.

Complex permeability

A useful tool for dealing with high frequency magnetic effects is the complex permeability. While at low frequencies in a linear material the magnetic field and the auxiliary magnetic field are simply proportional to each other through some scalar permeability, at high frequencies these quantities will react to each other with some lag time. These fields can be written as phasors, such that

${\displaystyle H=H_0{e}^{j\omega t}B=B_0{e}^{j\left(\omega t-\delta \right)}}$

where ${\displaystyle \delta }$ is the phase delay of ${\displaystyle B}$ from ${\displaystyle H}$.

Understanding permeability as the ratio of the magnetic flux density to the magnetic field, the ratio of the phasors can be written and simplified as

${\displaystyle \mu =\frac{B}{H}=\frac{B_0{e}^{j\left(\omega t-\delta \right)}}{H_0{e}^{j\omega t}}=\frac{B_0}{H_0}{e}^{-j\delta },}$

so that the permeability becomes a complex number.

By Euler's formula, the complex permeability can be translated from polar to rectangular form,

${\displaystyle \mu =\frac{B_0}{H_0}\cos (\delta )-j\frac{B_0}{H_0}\sin (\delta )={\mu }^{\prime }-j{\mu }^{″}.}$

The ratio of the imaginary to the real part of the complex permeability is called the loss tangent,

${\displaystyle \tan (\delta )=\frac{{\mu }^{″}}{{\mu }^{\prime }},}$

which provides a measure of how much power is lost in material versus how much is stored.

Blood substitute

From Wikipedia, the free encyclopedia

https://en.wikipedia.org/wiki/Blood_substitute

A blood substitute (also called artificial blood or blood surrogate) is a substance used to mimic and fulfill some functions of biological blood. It aims to provide an alternative to blood transfusion, which is transferring blood or blood-based products from one person into another. Thus far, there are no well-accepted oxygen-carrying blood substitutes, which is the typical objective of a red blood cell transfusion; however, there are widely available non-blood volume expanders for cases where only volume restoration is required. These are helping doctors and surgeons avoid the risks of disease transmission and immune suppression, address the chronic blood donor shortage, and address the concerns of Jehovah's Witnesses and others who have religious objections to receiving transfused blood.

The main categories of "oxygen-carrying" blood substitutes being pursued are hemoglobin-based oxygen carriers (HBOC) and perfluorocarbon emulsions. Oxygen therapeutics are in clinical trials in the U.S. and European Union, and Hemopure is available in South Africa.

History

After William Harvey discovered blood pathways in 1616, many people tried to use fluids such as beer, urine, milk, and non-human animal blood as blood substitute. Sir Christopher Wren suggested wine and opium as blood substitute.

At the beginning of the 20th century, the development of modern transfusion medicine initiated through the work of Landsteiner and co-authors opened the possibility to understanding the general principle of blood group serology. Simultaneously, significant progress was made in the fields of heart and circulation physiology as well as in the understanding of the mechanism of oxygen transport and tissue oxygenation.

Restrictions in applied transfusion medicine, especially in disaster situations such as World War II, laid the grounds for accelerated research in the field of blood substitutes. Early attempts and optimism in developing blood substitutes were very quickly confronted with significant side effects, which could not be promptly eliminated due to the level of knowledge and technology available at that time. The emergence of HIV in the 1980s renewed impetus for development of infection-safe blood substitutes. Public concern about the safety of the blood supply was raised further by mad cow disease. The continuous decline of blood donation combined with the increased demand for blood transfusion (increased ageing of population, increased incidence of invasive diagnostic, chemotherapy and extensive surgical interventions, terror attacks, international military conflicts) and positive estimation of investors in biotechnology branch made for a positive environment for further development of blood substitutes.

Efforts to develop blood substitutes have been driven by a desire to replace blood transfusion in emergency situations, in places where infectious disease is endemic and the risk of contaminated blood products is high, where refrigeration to preserve blood may be lacking, and where it might not be possible or convenient to find blood type matches.

In 2023, DARPA announced funding twelve universities and labs for synthetic blood research. Human trials would be expected to 2028~2030.

Approaches

Efforts have focused on molecules that can carry oxygen, and most work has focused on recombinant hemoglobin, which normally carries oxygen, and perfluorocarbons (PFC), chemical compounds which can carry and release oxygen.

The first approved oxygen-carrying blood substitute was a perfluorocarbon-based product called Fluosol-DA-20, manufactured by Green Cross of Japan. It was approved by the Food and Drug Administration (FDA) in 1989. Because of limited success, complexity of use and side effects, it was withdrawn in 1994. However, Fluosol-DA remains the only oxygen therapeutic ever fully approved by the FDA. As of 2017 no hemoglobin-based product had been approved.

Perfluorocarbon based

Perfluorochemicals are not water soluble and will not mix with blood, therefore emulsions must be made by dispersing small drops of PFC in water. This liquid is then mixed with antibiotics, vitamins, nutrients and salts, producing a mixture that contains about 80 different components, and performs many of the vital functions of natural blood. PFC particles are about 1/40 the size of the diameter of a red blood cell (RBC). This small size can enable PFC particles to traverse capillaries through which no RBCs are flowing. In theory this can benefit damaged, blood-starved tissue, which conventional red cells cannot reach. PFC solutions can carry oxygen so well that mammals, including humans, can survive breathing liquid PFC solution, called liquid breathing.

Perfluorocarbon-based blood substitutes are completely man-made; this provides advantages over blood substitutes that rely on modified hemoglobin, such as unlimited manufacturing capabilities, ability to be heat-sterilized, and PFCs' efficient oxygen delivery and carbon dioxide removal. PFCs in solution act as an intravascular oxygen carrier to temporarily augment oxygen delivery to tissues. PFCs are removed from the bloodstream within 48 hours by the body's normal clearance procedure for particles in the blood – exhalation. PFC particles in solution can carry several times more oxygen per cubic centimeter (cc) than blood, while being 40 to 50 times smaller than hemoglobin.

Fluosol was made mostly of perfluorodecalin or perfluorotributylamine suspended in an albumin emulsion. It was developed in Japan and first tested in the United States in November 1979. In order to "load" sufficient amounts of oxygen into it, people who had been given it had to breathe pure oxygen by mask or in a hyperbaric chamber. It was approved by the FDA in 1989, and was approved in eight other countries. Its use was associated with a reduction in ischemic complications and with an increase in pulmonary edema and congestive heart failure. Due to difficulty with the emulsion storage of Fluosol use (frozen storage and rewarming), its popularity declined and its production ended in 1994.

Name	Sponsor	Description
Oxycyte	Oxygen Biotherapeutics	Tested in a Phase II-b Trials in the United States. Targeted as an oxygen therapeutic rather than a blood substitute, with successful small-scale open label human trials treating traumatic brain injury at Virginia Commonwealth University. The trial was later terminated.
PHER-O 2	Sanguine Corp	In research
Perftoran	Russia	Contains perfluorodecalin and perfluoro-N-(4-methylcyclohexyl)-piperidine along with a surfactant, Proxanol-268. It was developed in Russia and as of 2005 was marketed there.
NVX-108	NuvOx Pharma	In a Phase Ib/II clinical trial where it raises tumor oxygen levels prior to radiation therapy in order to radiosensitize them.

Oxygent was a second-generation, lecithin-stabilized emulsion of a PFC that was under development by Alliance Pharmaceuticals. In 2002 a Phase III study was halted early due an increase in incidences of strokes in the study arm.

Haemoglobin based

Haemoglobin is the main component of red blood cells, comprising about 33% of the cell mass. Haemoglobin-based products are called haemoglobin-based oxygen carriers (HBOCs).

Unmodified cell-free haemoglobin is not useful as a blood substitute because its oxygen affinity is too high for effective tissue oxygenation, the half-life within the intravascular space that is too short to be clinically useful, it has a tendency to undergo dissociation in dimers with resultant kidney damage and toxicity, and because free haemoglobin tends to take up nitric oxide, causing vasoconstriction.

Efforts to overcome this toxicity have included making genetically engineered versions, cross-linking, polymerization, and encapsulation.

HemAssist, a diaspirin cross-linked haemoglobin (DCLHb) was developed by Baxter Healthcare; it was the most widely studied of the haemoglobin-based blood substitutes, used in more than a dozen animal and clinical studies. It reached Phase III clinical trials, in which it failed due to increased mortality in the trial arm, mostly due to severe vasoconstriction complications. The results were published in 1999.

Hemolink (Hemosol Inc., Mississauga, Canada) was a haemoglobin solution that contained cross-linked an o-rafinose polymerised human haemoglobin. Hemosol struggled after Phase II trials were halted in 2003 on safety concerns and declared bankruptcy in 2005.

Hemopure was developed by Biopure Corp and was a chemically stabilized, cross-linked bovine (cow) haemoglobin in a salt solution intended for human use; the company developed the same product under the trade name Oxyglobin for veterinary use in dogs. Oxyglobin was approved in the US and Europe and was introduced to veterinary clinics and hospitals in March 1998. Hemopure was approved in South Africa and Russia. Biopure filed for bankruptcy protection in 2009. Its assets were subsequently purchased by HbO2 Therapeutics in 2014.

PolyHeme was developed over 20 years by Northfield Laboratories and began as a military project following the Vietnam War. It is human haemoglobin, extracted from red blood cells, then polymerized, then incorporated into an electrolyte solution. In April 2009, the FDA rejected Northfield's Biologic License Application and in June 2009, Northfield filed for bankruptcy.

Dextran-Haemoglobin was developed by Dextro-Sang Corp as a veterinary product, and was a conjugate of the polymer dextran with human haemoglobin.

Hemotech was developed by HemoBiotech and was a chemically modified haemoglobin.

Somatogen developed a genetically engineered and crosslinked tetramer it called Optro. It failed in a phase II trial that was published in 2014 and development was halted.

A pyridoxylated Hb conjugated with polyoxyethylene was created by scientists at Ajinomoto and eventually developed by Apex Biosciences, a subsidiary of Curacyte AG; it was called "PHP" and failed in a Phase III trial published in 2014, due to increased mortality in the control arm, which led to Curacyte shutting down.

Similarly, Hemospan was developed by Sangart, and was a pegylated haemoglobin provided in a powdered form. While early trials were promising Sangart ran out of funding and closed down.

Stem cells

Stem cells offer a possible means of producing transfusable blood. A study performed by Giarratana et al. describes a large-scale ex-vivo production of mature human blood cells using hematopoietic stem cells. The cultured cells possessed the same haemoglobin content and morphology as native red blood cells. The authors contend that the cells had a near-normal lifespan, when compared to natural red blood cells.

Scientists from the experimental arm of the United States Department of Defense began creating artificial blood for use in remote areas and transfuse blood to wounded soldiers more quickly in 2010. The blood is made from the hematopoietic stem cells removed from the umbilical cord between human mother and newborn using a method called blood pharming. Pharming has been used in the past on animals and plants to create medical substances in large quantities. Each cord can produce approximately 20 units of blood. The blood is being produced for the Defense Advanced Research Projects Agency by Arteriocyte. The Food and Drug Administration has examined and approved the safety of this blood from previously submitted O-negative blood. Using this particular artificial blood will reduce the costs per unit of blood from $5,000 to equal or less than $1,000. This blood will also serve as a blood donor to all common blood types.

Glacier

From Wikipedia, the free encyclopedia

https://en.wikipedia.org/wiki/Glacier

Glacier of the Geikie Plateau in Greenland.

The Taschachferner in the Ötztal Alps in Austria. The mountain to the left is the Wildspitze (3.768 m), second highest in Austria. To the right is an area with open crevasses where the glacier flows over a kind of large cliff. The distance from left to right image border is c. 1.5 km in reality.

A glacier (US: /ˈɡleɪʃər/; UK: /ˈɡlæsiər, ˈɡleɪsiər/) is a persistent body of dense ice that is constantly moving under its own weight. A glacier forms where the accumulation of snow exceeds its ablation over many years, often centuries. It acquires distinguishing features, such as crevasses and seracs, as it slowly flows and deforms under stresses induced by its weight. As it moves, it abrades rock and debris from its substrate to create landforms such as cirques, moraines, or fjords. Although a glacier may flow into a body of water, it forms only on land and is distinct from the much thinner sea ice and lake ice that form on the surface of bodies of water.

On Earth, 99% of glacial ice is contained within vast ice sheets (also known as "continental glaciers") in the polar regions, but glaciers may be found in mountain ranges on every continent other than the Australian mainland, including Oceania's high-latitude oceanic island countries such as New Zealand. Between latitudes 35°N and 35°S, glaciers occur only in the Himalayas, Andes, and a few high mountains in East Africa, Mexico, New Guinea and on Zard-Kuh in Iran. With more than 7,000 known glaciers, Pakistan has more glacial ice than any other country outside the polar regions. Glaciers cover about 10% of Earth's land surface. Continental glaciers cover nearly 13 million km² (5 million sq mi) or about 98% of Antarctica's 13.2 million km² (5.1 million sq mi), with an average thickness of ice 2,100 m (7,000 ft). Greenland and Patagonia also have huge expanses of continental glaciers. The volume of glaciers, not including the ice sheets of Antarctica and Greenland, has been estimated at 170,000 km³.

Glacial ice is the largest reservoir of fresh water on Earth, holding with ice sheets about 69 percent of the world's freshwater. Many glaciers from temperate, alpine and seasonal polar climates store water as ice during the colder seasons and release it later in the form of meltwater as warmer summer temperatures cause the glacier to melt, creating a water source that is especially important for plants, animals and human uses when other sources may be scant. However, within high-altitude and Antarctic environments, the seasonal temperature difference is often not sufficient to release meltwater.

Since glacial mass is affected by long-term climatic changes, e.g., precipitation, mean temperature, and cloud cover, glacial mass changes are considered among the most sensitive indicators of climate change and are a major source of variations in sea level.

A large piece of compressed ice, or a glacier, appears blue, as large quantities of water appear blue. This is because water molecules absorb other colors more efficiently than blue. The other reason for the blue color of glaciers is the lack of air bubbles. Air bubbles, which give a white color to ice, are squeezed out by pressure increasing the created ice's density.

Etymology and related terms

The word glacier is a loanword from French and goes back, via Franco-Provençal, to the Vulgar Latin glaciārium, derived from the Late Latin glacia, and ultimately Latin glaciēs, meaning "ice". The processes and features caused by or related to glaciers are referred to as glacial. The process of glacier establishment, growth and flow is called glaciation. The corresponding area of study is called glaciology. Glaciers are important components of the global cryosphere.

Types

Classification by size, shape and behavior

Further information: Glacier morphology

The Quelccaya Ice Cap in Peru is the second-largest glaciated area in the tropics

Glaciers are categorized by their morphology, thermal characteristics, and behavior. Alpine glaciers form on the crests and slopes of mountains. A glacier that fills a valley is called a valley glacier, or alternatively, an alpine glacier or mountain glacier. A large body of glacial ice astride a mountain, mountain range, or volcano is termed an ice cap or ice field. Ice caps have an area less than 50,000 km² (19,000 sq mi) by definition.

Glacial bodies larger than 50,000 km² (19,000 sq mi) are called ice sheets or continental glaciers. Several kilometers deep, they obscure the underlying topography. Only nunataks protrude from their surfaces. The only extant ice sheets are the two that cover most of Antarctica and Greenland. They contain vast quantities of freshwater, enough that if both melted, global sea levels would rise by over 70 m (230 ft). Portions of an ice sheet or cap that extend into water are called ice shelves; they tend to be thin with limited slopes and reduced velocities. Narrow, fast-moving sections of an ice sheet are called ice streams. In Antarctica, many ice streams drain into large ice shelves. Some drain directly into the sea, often with an ice tongue, like Mertz Glacier.

Tidewater glaciers are glaciers that terminate in the sea, including most glaciers flowing from Greenland, Antarctica, Baffin, Devon, and Ellesmere Islands in Canada, Southeast Alaska, and the Northern and Southern Patagonian Ice Fields. As the ice reaches the sea, pieces break off or calve, forming icebergs. Most tidewater glaciers calve above sea level, which often results in a tremendous impact as the iceberg strikes the water. Tidewater glaciers undergo centuries-long cycles of advance and retreat that are much less affected by climate change than other glaciers.

Classification by thermal state

Webber Glacier on Grant Land is an advancing polar glacier

Thermally, a temperate glacier is at a melting point throughout the year, from its surface to its base. The ice of a polar glacier is always below the freezing threshold from the surface to its base, although the surface snowpack may experience seasonal melting. A subpolar glacier includes both temperate and polar ice, depending on the depth beneath the surface and position along the length of the glacier. In a similar way, the thermal regime of a glacier is often described by its basal temperature. A cold-based glacier is below freezing at the ice-ground interface and is thus frozen to the underlying substrate. A warm-based glacier is above or at freezing at the interface and is able to slide at this contact. This contrast is thought to a large extent to govern the ability of a glacier to effectively erode its bed, as sliding ice promotes plucking at rock from the surface below. Glaciers which are partly cold-based and partly warm-based are known as polythermal.

Formation

A glacier cave located on the Perito Moreno Glacier in Argentina

Glaciers form where the accumulation of snow and ice exceeds ablation. A glacier usually originates from a cirque landform (alternatively known as a corrie or as a cwm) – a typically armchair-shaped geological feature (such as a depression between mountains enclosed by arêtes) – which collects and compresses through gravity the snow that falls into it. This snow accumulates and the weight of the snow falling above compacts it, forming névé (granular snow). Further crushing of the individual snowflakes and squeezing the air from the snow turns it into "glacial ice". This glacial ice will fill the cirque until it "overflows" through a geological weakness or vacancy, such as a gap between two mountains. When the mass of snow and ice reaches sufficient thickness, it begins to move by a combination of surface slope, gravity, and pressure. On steeper slopes, this can occur with as little as 15 m (49 ft) of snow-ice.

In temperate glaciers, snow repeatedly freezes and thaws, changing into granular ice called firn. Under the pressure of the layers of ice and snow above it, this granular ice fuses into denser firn. Over a period of years, layers of firn undergo further compaction and become glacial ice. Glacier ice is slightly more dense than ice formed from frozen water because glacier ice contains fewer trapped air bubbles.

Glacial ice has a distinctive blue tint because it absorbs some red light due to an overtone of the infrared OH stretching mode of the water molecule. (Liquid water appears blue for the same reason. The blue of glacier ice is sometimes misattributed to Rayleigh scattering of bubbles in the ice.)

Structure

Black ice glacier near Aconcagua, Argentina

A glacier originates at a location called its glacier head and terminates at its glacier foot, snout, or terminus.

Glaciers are broken into zones based on surface snowpack and melt conditions. The ablation zone is the region where there is a net loss in glacier mass. The upper part of a glacier, where accumulation exceeds ablation, is called the accumulation zone. The equilibrium line separates the ablation zone and the accumulation zone; it is the contour where the amount of new snow gained by accumulation is equal to the amount of ice lost through ablation. In general, the accumulation zone accounts for 60–70% of the glacier's surface area, more if the glacier calves icebergs. Ice in the accumulation zone is deep enough to exert a downward force that erodes underlying rock. After a glacier melts, it often leaves behind a bowl- or amphitheater-shaped depression that ranges in size from large basins like the Great Lakes to smaller mountain depressions known as cirques.

The accumulation zone can be subdivided based on its melt conditions.

1. The dry snow zone is a region where no melt occurs, even in the summer, and the snowpack remains dry.
2. The percolation zone is an area with some surface melt, causing meltwater to percolate into the snowpack. This zone is often marked by refrozen ice lenses, glands, and layers. The snowpack also never reaches the melting point.
3. Near the equilibrium line on some glaciers, a superimposed ice zone develops. This zone is where meltwater refreezes as a cold layer in the glacier, forming a continuous mass of ice.
4. The wet snow zone is the region where all of the snow deposited since the end of the previous summer has been raised to 0 °C.

The health of a glacier is usually assessed by determining the glacier mass balance or observing terminus behavior. Healthy glaciers have large accumulation zones, more than 60% of their area is snow-covered at the end of the melt season, and they have a terminus with a vigorous flow.

Following the Little Ice Age's end around 1850, glaciers around the Earth have retreated substantially. A slight cooling led to the advance of many alpine glaciers between 1950 and 1985, but since 1985 glacier retreat and mass loss has become larger and increasingly ubiquitous.

Motion

Main article: Ice-sheet dynamics

Shear or herring-bone crevasses on Emmons Glacier (Mount Rainier); such crevasses often form near the edge of a glacier where interactions with underlying or marginal rock impede flow. In this case, the impediment appears to be some distance from the near margin of the glacier.

The overhanging icefront of the advancing Webber Glacier with waterfalls (Borup Fiord area, Northern Ellesmere Island). Debris rich layers have been sheared and folded into the basal cold glacier ice. The glacier front is 6 km broad and up to 40 m high. July 20, 1978,

Glaciers move, or flow, downhill by the force of gravity and the internal deformation of ice. Ice behaves like a brittle solid until its thickness exceeds about 50 m (160 ft). The pressure on ice deeper than 50 m causes plastic flow. At the molecular level, ice consists of stacked layers of molecules with relatively weak bonds between layers. When the stress on the layer above exceeds the inter-layer binding strength, it moves faster than the layer below.

Glaciers also move through basal sliding. In this process, a glacier slides over the terrain on which it sits, lubricated by the presence of liquid water. The water is created from ice that melts under high pressure from frictional heating. Basal sliding is dominant in temperate or warm-based glaciers.

Although evidence in favor of glacial flow was known by the early 19th century, other theories of glacial motion were advanced, such as the idea that meltwater, refreezing inside glaciers, caused the glacier to dilate and extend its length. As it became clear that glaciers behaved to some degree as if the ice were a viscous fluid, it was argued that "regelation", or the melting and refreezing of ice at a temperature lowered by the pressure on the ice inside the glacier, was what allowed the ice to deform and flow. James Forbes came up with the essentially correct explanation in the 1840s, although it was several decades before it was fully accepted.

Fracture zone and cracks

Ice cracks in the Titlis Glacier

The top 50 m (160 ft) of a glacier are rigid because they are under low pressure. This upper section is known as the fracture zone and moves mostly as a single unit over the plastic-flowing lower section. When a glacier moves through irregular terrain, cracks called crevasses develop in the fracture zone. Crevasses form because of differences in glacier velocity. If two rigid sections of a glacier move at different speeds or directions, shear forces cause them to break apart, opening a crevasse. Crevasses are seldom more than 46 m (150 ft) deep but, in some cases, can be at least 300 m (1,000 ft) deep. Beneath this point, the plasticity of the ice prevents the formation of cracks. Intersecting crevasses can create isolated peaks in the ice, called seracs.

Crevasses can form in several different ways. Transverse crevasses are transverse to flow and form where steeper slopes cause a glacier to accelerate. Longitudinal crevasses form semi-parallel to flow where a glacier expands laterally. Marginal crevasses form near the edge of the glacier, caused by the reduction in speed caused by friction of the valley walls. Marginal crevasses are largely transverse to flow. Moving glacier ice can sometimes separate from the stagnant ice above, forming a bergschrund. Bergschrunds resemble crevasses but are singular features at a glacier's margins. Crevasses make travel over glaciers hazardous, especially when they are hidden by fragile snow bridges.

Below the equilibrium line, glacial meltwater is concentrated in stream channels. Meltwater can pool in proglacial lakes on top of a glacier or descend into the depths of a glacier via moulins. Streams within or beneath a glacier flow in englacial or sub-glacial tunnels. These tunnels sometimes reemerge at the glacier's surface.

Speed

The speed of glacial displacement is partly determined by friction. Friction makes the ice at the bottom of the glacier move more slowly than ice at the top. In alpine glaciers, friction is also generated at the valley's sidewalls, which slows the edges relative to the center.

Mean glacial speed varies greatly but is typically around 1 m (3 ft) per day. There may be no motion in stagnant areas; for example, in parts of Alaska, trees can establish themselves on surface sediment deposits. In other cases, glaciers can move as fast as 20–30 m (70–100 ft) per day, such as in Greenland's Jakobshavn Isbræ. Glacial speed is affected by factors such as slope, ice thickness, snowfall, longitudinal confinement, basal temperature, meltwater production, and bed hardness.

A few glaciers have periods of very rapid advancement called surges. These glaciers exhibit normal movement until suddenly they accelerate, then return to their previous movement state. These surges may be caused by the failure of the underlying bedrock, the pooling of meltwater at the base of the glacier — perhaps delivered from a supraglacial lake — or the simple accumulation of mass beyond a critical "tipping point". Temporary rates up to 90 m (300 ft) per day have occurred when increased temperature or overlying pressure caused bottom ice to melt and water to accumulate beneath a glacier.

In glaciated areas where the glacier moves faster than one km per year, glacial earthquakes occur. These are large scale earthquakes that have seismic magnitudes as high as 6.1. The number of glacial earthquakes in Greenland peaks every year in July, August, and September and increased rapidly in the 1990s and 2000s. In a study using data from January 1993 through October 2005, more events were detected every year since 2002, and twice as many events were recorded in 2005 as there were in any other year.

Ogives

Forbes bands on the Mer de Glace glacier in France

Ogives or Forbes bands are alternating wave crests and valleys that appear as dark and light bands of ice on glacier surfaces. They are linked to seasonal motion of glaciers; the width of one dark and one light band generally equals the annual movement of the glacier. Ogives are formed when ice from an icefall is severely broken up, increasing ablation surface area during summer. This creates a swale and space for snow accumulation in the winter, which in turn creates a ridge. Sometimes ogives consist only of undulations or color bands and are described as wave ogives or band ogives.

Geography

Further information on this topic: List of glaciers

Fox Glacier in New Zealand finishes near a rainforest

Glaciers are present on every continent and in approximately fifty countries, excluding those (Australia, South Africa) that have glaciers only on distant subantarctic island territories. Extensive glaciers are found in Antarctica, Argentina, Chile, Canada, Alaska, Greenland and Iceland. Mountain glaciers are widespread, especially in the Andes, the Himalayas, the Rocky Mountains, the Caucasus, Scandinavian mountains, and the Alps. Snezhnika glacier in Pirin Mountain, Bulgaria with a latitude of 41°46′09″ N is the southernmost glacial mass in Europe. Mainland Australia currently contains no glaciers, although a small glacier on Mount Kosciuszko was present in the last glacial period. In New Guinea, small, rapidly diminishing, glaciers are located on Puncak Jaya. Africa has glaciers on Mount Kilimanjaro in Tanzania, on Mount Kenya, and in the Rwenzori Mountains. Oceanic islands with glaciers include Iceland, several of the islands off the coast of Norway including Svalbard and Jan Mayen to the far north, New Zealand and the subantarctic islands of Marion, Heard, Grande Terre (Kerguelen) and Bouvet. During glacial periods of the Quaternary, Taiwan, Hawaii on Mauna Kea and Tenerife also had large alpine glaciers, while the Faroe and Crozet Islands were completely glaciated.

The permanent snow cover necessary for glacier formation is affected by factors such as the degree of slope on the land, amount of snowfall and the winds. Glaciers can be found in all latitudes except from 20° to 27° north and south of the equator where the presence of the descending limb of the Hadley circulation lowers precipitation so much that with high insolation snow lines reach above 6,500 m (21,330 ft). Between 19˚N and 19˚S, however, precipitation is higher, and the mountains above 5,000 m (16,400 ft) usually have permanent snow.

Even at high latitudes, glacier formation is not inevitable. Areas of the Arctic, such as Banks Island, and the McMurdo Dry Valleys in Antarctica are considered polar deserts where glaciers cannot form because they receive little snowfall despite the bitter cold. Cold air, unlike warm air, is unable to transport much water vapor. Even during glacial periods of the Quaternary, Manchuria, lowland Siberia, and central and northern Alaska, though extraordinarily cold, had such light snowfall that glaciers could not form.

In addition to the dry, unglaciated polar regions, some mountains and volcanoes in Bolivia, Chile and Argentina are high (4,500 to 6,900 m or 14,800 to 22,600 ft) and cold, but the relative lack of precipitation prevents snow from accumulating into glaciers. This is because these peaks are located near or in the hyperarid Atacama Desert.

Glacial geology

Diagram of glacial plucking and abrasion

Glaciers erode terrain through two principal processes: plucking and abrasion.

As glaciers flow over bedrock, they soften and lift blocks of rock into the ice. This process, called plucking, is caused by subglacial water that penetrates fractures in the bedrock and subsequently freezes and expands. This expansion causes the ice to act as a lever that loosens the rock by lifting it. Thus, sediments of all sizes become part of the glacier's load. If a retreating glacier gains enough debris, it may become a rock glacier, like the Timpanogos Glacier in Utah.

Abrasion occurs when the ice and its load of rock fragments slide over bedrock and function as sandpaper, smoothing and polishing the bedrock below. The pulverized rock this process produces is called rock flour and is made up of rock grains between 0.002 and 0.00625 mm in size. Abrasion leads to steeper valley walls and mountain slopes in alpine settings, which can cause avalanches and rock slides, which add even more material to the glacier. Glacial abrasion is commonly characterized by glacial striations. Glaciers produce these when they contain large boulders that carve long scratches in the bedrock. By mapping the direction of the striations, researchers can determine the direction of the glacier's movement. Similar to striations are chatter marks, lines of crescent-shape depressions in the rock underlying a glacier. They are formed by abrasion when boulders in the glacier are repeatedly caught and released as they are dragged along the bedrock.

Glacially plucked granitic bedrock near Mariehamn, Åland

The rate of glacier erosion varies. Six factors control erosion rate:

• Velocity of glacial movement
• Thickness of the ice
• Shape, abundance and hardness of rock fragments contained in the ice at the bottom of the glacier
• Relative ease of erosion of the surface under the glacier
• Thermal conditions at the glacier base
• Permeability and water pressure at the glacier base

When the bedrock has frequent fractures on the surface, glacial erosion rates tend to increase as plucking is the main erosive force on the surface; when the bedrock has wide gaps between sporadic fractures, however, abrasion tends to be the dominant erosive form and glacial erosion rates become slow. Glaciers in lower latitudes tend to be much more erosive than glaciers in higher latitudes, because they have more meltwater reaching the glacial base and facilitate sediment production and transport under the same moving speed and amount of ice.

Material that becomes incorporated in a glacier is typically carried as far as the zone of ablation before being deposited. Glacial deposits are of two distinct types:

• Glacial till: material directly deposited from glacial ice. Till includes a mixture of undifferentiated material ranging from clay size to boulders, the usual composition of a moraine.
• Fluvial and outwash sediments: sediments deposited by water. These deposits are stratified by size.

Larger pieces of rock that are encrusted in till or deposited on the surface are called "glacial erratics". They range in size from pebbles to boulders, but as they are often moved great distances, they may be drastically different from the material upon which they are found. Patterns of glacial erratics hint at past glacial motions.

Moraines

Glacial moraines above Lake Louise, Alberta, Canada

Glacial moraines are formed by the deposition of material from a glacier and are exposed after the glacier has retreated. They usually appear as linear mounds of till, a non-sorted mixture of rock, gravel, and boulders within a matrix of fine powdery material. Terminal or end moraines are formed at the foot or terminal end of a glacier. Lateral moraines are formed on the sides of the glacier. Medial moraines are formed when two different glaciers merge and the lateral moraines of each coalesce to form a moraine in the middle of the combined glacier. Less apparent are ground moraines, also called glacial drift, which often blankets the surface underneath the glacier downslope from the equilibrium line. The term moraine is of French origin. It was coined by peasants to describe alluvial embankments and rims found near the margins of glaciers in the French Alps. In modern geology, the term is used more broadly and is applied to a series of formations, all of which are composed of till. Moraines can also create moraine-dammed lakes.

Drumlins

Drumlins around Horicon Marsh, Wisconsin, in an area with one of the highest concentration of drumlins in the world. The curved path of the Laurentide Ice Sheet is evident in the orientation of the various mounds.

Drumlins are asymmetrical, canoe-shaped hills made mainly of till. Their heights vary from 15 to 50 meters, and they can reach a kilometer in length. The steepest side of the hill faces the direction from which the ice advanced (stoss), while a longer slope is left in the ice's direction of movement (lee). Drumlins are found in groups called drumlin fields or drumlin camps. One of these fields is found east of Rochester, New York; it is estimated to contain about 10,000 drumlins. Although the process that forms drumlins is not fully understood, their shape implies that they are products of the plastic deformation zone of ancient glaciers. It is believed that many drumlins were formed when glaciers advanced over and altered the deposits of earlier glaciers.

Glacial valleys, cirques, arêtes, and pyramidal peaks

Features of a glacial landscape

Before glaciation, mountain valleys have a characteristic "V" shape, produced by eroding water. During glaciation, these valleys are often widened, deepened and smoothed to form a "U"-shaped glacial valley or glacial trough, as it is sometimes called. The erosion that creates glacial valleys truncates any spurs of rock or earth that may have earlier extended across the valley, creating broadly triangular-shaped cliffs called truncated spurs. Within glacial valleys, depressions created by plucking and abrasion can be filled by lakes, called paternoster lakes. If a glacial valley runs into a large body of water, it forms a fjord.

Typically glaciers deepen their valleys more than their smaller tributaries. Therefore, when glaciers recede, the valleys of the tributary glaciers remain above the main glacier's depression and are called hanging valleys.

At the start of a classic valley glacier is a bowl-shaped cirque, which have escarped walls on three sides but is open on the side that descends into the valley. Cirques are where ice begins to accumulate in a glacier. Two glacial cirques may form back to back and erode their backwalls until only a narrow ridge, called an arête is left. This structure may result in a mountain pass. If multiple cirques encircle a single mountain, they create pointed pyramidal peaks; particularly steep examples are called horns.

Roches moutonnées

Passage of glacial ice over an area of bedrock may cause the rock to be sculpted into a knoll called a roche moutonnée, or "sheepback" rock. Roches moutonnées may be elongated, rounded and asymmetrical in shape. They range in length from less than a meter to several hundred meters long. Roches moutonnées have a gentle slope on their up-glacier sides and a steep to vertical face on their down-glacier sides. The glacier abrades the smooth slope on the upstream side as it flows along, but tears rock fragments loose and carries them away from the downstream side via plucking.

Alluvial stratification

As the water that rises from the ablation zone moves away from the glacier, it carries fine eroded sediments with it. As the speed of the water decreases, so does its capacity to carry objects in suspension. The water thus gradually deposits the sediment as it runs, creating an alluvial plain. When this phenomenon occurs in a valley, it is called a valley train. When the deposition is in an estuary, the sediments are known as bay mud. Outwash plains and valley trains are usually accompanied by basins known as "kettles". These are small lakes formed when large ice blocks that are trapped in alluvium melt and produce water-filled depressions. Kettle diameters range from 5 m to 13 km, with depths of up to 45 meters. Most are circular in shape because the blocks of ice that formed them were rounded as they melted.

Glacial deposits

Landscape produced by a receding glacier

When a glacier's size shrinks below a critical point, its flow stops and it becomes stationary. Meanwhile, meltwater within and beneath the ice leaves stratified alluvial deposits. These deposits, in the forms of columns, terraces and clusters, remain after the glacier melts and are known as "glacial deposits". Glacial deposits that take the shape of hills or mounds are called kames. Some kames form when meltwater deposits sediments through openings in the interior of the ice. Others are produced by fans or deltas created by meltwater. When the glacial ice occupies a valley, it can form terraces or kames along the sides of the valley. Long, sinuous glacial deposits are called eskers. Eskers are composed of sand and gravel that was deposited by meltwater streams that flowed through ice tunnels within or beneath a glacier. They remain after the ice melts, with heights exceeding 100 meters and lengths of as long as 100 km.

Loess deposits

Very fine glacial sediments or rock flour is often picked up by wind blowing over the bare surface and may be deposited great distances from the original fluvial deposition site. These eolian loess deposits may be very deep, even hundreds of meters, as in areas of China and the Midwestern United States. Katabatic winds can be important in this process.

Climate change

Further information: Retreat of glaciers since 1850

 

South Cascade Glacier in Washington photographs from 1928 to 2003 showing the recent rapid glacier retreating

 

Based on current national pledges, global average temperature increase is projected to cause loss of ~half of Earth's glaciers by 2100 and raise sea level by ~115 mm (not counting rise from melting ice sheets).

Glaciers, which can be hundreds of thousands of years old, are used to track climate change over long periods of time. Researchers melt or crush samples from glacier ice cores whose progressively deep layers represent respectively earlier times in Earth's climate history. The researchers apply various instruments to the content of bubbles trapped in the cores' layers in order to track changes in the atmosphere's composition. Temperatures are deduced from differing relative concentrations of respective gases, confirming that for at least the last million years, global temperatures have been linked to carbon dioxide concentrations.

Human activities in the industrial era have increased the concentration of carbon dioxide and other heat-trapping greenhouse gases in the air, causing current global warming. Human influence is the principal driver of changes to the cryosphere of which glaciers are a part.

Global warming creates positive feedback loops with glaciers. For example, in ice–albedo feedback, rising temperatures increase glacier melt, exposing more of earth's land and sea surface (which is darker than glacier ice), allowing sunlight to warm the surface rather than being reflected back into space. Reference glaciers tracked by the World Glacier Monitoring Service have lost ice every year since 1988.

Water runoff from melting glaciers causes global sea level to rise, a phenomenon the IPCC terms a "slow onset" event. Impacts at least partially attributable to sea level rise include encroachment on coastal settlements and infrastructure, increase in populations inhabiting 100-year coastal flood zones, existential threats to small islands and low-lying coasts, declines in coastal fishery resources, losses of coastal ecosystems and ecosystem services, groundwater salinization, increased risks to coastal food and water security, and compounding damage from tropical cyclones, flooding, storm surge, and land subsidence.

Isostatic rebound

Isostatic pressure by a glacier on the Earth's crust

Large masses, such as ice sheets or glaciers, can depress the crust of the Earth into the mantle. The depression usually totals a third of the ice sheet or glacier's thickness. After the ice sheet or glacier melts, the mantle begins to flow back to its original position, pushing the crust back up. This post-glacial rebound, which proceeds very slowly after the melting of the ice sheet or glacier, is currently occurring in measurable amounts in Scandinavia and the Great Lakes region of North America.

A geomorphological feature created by the same process on a smaller scale is known as dilation-faulting. It occurs where previously compressed rock is allowed to return to its original shape more rapidly than can be maintained without faulting. This leads to an effect similar to what would be seen if the rock were hit by a large hammer. Dilation faulting can be observed in recently de-glaciated parts of Iceland and Cumbria.

On Mars

Main article: Glaciers on Mars

Protonilus Mensae, Ismenius Lacus quadrangle, Mars

The polar ice caps of Mars show geologic evidence of glacial deposits. The south polar cap is especially comparable to glaciers on Earth. Topographical features and computer models indicate the existence of more glaciers in Mars' past. At mid-latitudes, between 35° and 65° north or south, Martian glaciers are affected by the thin Martian atmosphere. Because of the low atmospheric pressure, ablation near the surface is solely caused by sublimation, not melting. As on Earth, many glaciers are covered with a layer of rocks which insulates the ice. A radar instrument on board the Mars Reconnaissance Orbiter found ice under a thin layer of rocks in formations called lobate debris aprons (LDAs).