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[[Sea ice]] is a complex composite composed primarily of pure ice in various states of [[crystallization]] along with air bubbles and included pockets of [[brine]]. Understanding its '''growth processes''' is important both for [[climate]] scientists for use in [[simulation]]s as well [[remote sensing]] specialists since the composition and microstructural properties of the ice ultimately affect how it interacts with [[electromagnetic radiation]].
== Speedy Programs In Snow Tube Examined ==
[[File:Sea ice microstructure.svg|thumb|A thin section of sea ice seen through cross-polarized light. All crystals (they have different interference colors) contain inclusions of brine (saline solution) and air - these lie within the (0001) crystallographic plane.]]
[[File:Nilas Sea Ice1.jpg|thumb|Nilas Ice formation at sea.]]


Sea ice growth models for predicting the [[sea ice concentration|ice distribution]] and extent are also valuable for shipping concerns. An ice growth model can be combined with [[remote sensing]] measurements in an [[data assimilation|assimilation]] model as a means of generating more accurate [[sea ice concentration|ice charts]].
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==Overview==
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Several formation mechanisms of sea ice have been identified. At its earliest stages, sea ice
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consists of elongated, randomly oriented [[crystals]]. This is called [[frazil ice|frazil]] and mixed with water in
the unconsolidated state is known as [[grease ice]]. If wave and wind conditions are calm, these
crystals will consolidate at the surface and by selective pressure, begin to grow preferentially
in the downward direction, forming [[nilas]]. In more turbulent conditions, the frazil will consolidate
by mechanical action to form [[pancake ice]], which has a more random structure
<ref name="Maykut_etal1992">
{{cite journal
|author=G. Maykut, T. Grenfell, and W. Weeks
|year=1992
|title=On estimating spatial and temporal variations in the properties of ice in the polar oceans
|journal=Journal of Marine Systems
|volume=3
|pages=41–72
|bibcode = 1992JMS.....3...41M |doi = 10.1016/0924-7963(92)90030-C }}</ref>
<ref name="Tucker_etal1992">
{{cite book
| title=Microwave Remote Sensing of Sea Ice
| editors=W. B. Tucker, D. K. Prerovich, A. J. Gow, W. F. Weeks, M. R. Drinkwater
| publisher=American Geophysical Union}}
</ref>
Another common formation mechanism,
especially in the [[Antarctic]] where [[Precipitation (meteorology)|precipitation]] over sea ice is high, is from snow deposition: on
thin ice, the snow will weigh down the ice enough to cause flooding. Subsequent freezing will
form ice with a much more granular structure.
<ref name="Ehn_etal2007">
{{cite journal
|authors=K. J. Ehn, B. J. Hwang, R. Galley, and D. G. Barber, D. G.
|year=2007
|title=Investigations of newly formed sea ice in the Cape Bathurst polynya: 1. Structural, physical and optical properties
|journal=Journal of Geophysical Research,
|volume=112
|number=C05002
|doi=10.1029/2006JC003702
|bibcode=2007JGRC..11205002E
}}</ref>
<ref name="Maksym_Markus2008">
{{cite journal
|author=T. Maksym and T. Markus
|year=2008
|title=Antarctic sea ice thickness and snow-to-ice conversion from atmospheric reanalysis and passive microwave snow depth
|journal=Journal of Geophysical Research
|volume=113
|number=C02S12
|doi=10.1029/2006JC004085
|bibcode=2008JGRC..11302S12M
}}</ref>
<ref name="Tang_etal2007">
{{cite journal
|author=S. Tang, D. Qin, J. Ren, J. Kang, and Z. Li
|year=2007
|title=Structure, salinity and isotopic composition of multi-year landfast sea ice in Nella Fjord, Antarctica
|journal=Cold Regions Science and Technology
|volume=49
|pages=170–177
}}</ref>


One of the more interesting processes to occur within consolidated ice packs is changes in
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the [[salinity|saline]] content. As the ice freezes, most of the [[salt]] content gets rejected and forms highly
saline [[brine]] inclusions between the [[crystals]]. With decreasing temperatures in the ice sheet, the
size of the brine pockets decreases while the salt content goes up. Since ice is less [[density|dense]] than
water, increasing [[pressure]] causes some of the brine to be ejected from both the top and bottom,
producing the characteristic ‘C’-shaped salinity profile of first year ice.
<ref name="Eicken1992">
{{cite journal
|author=Hajo Eicken
|year=1992
|title=Salinity Profiles of Antarctic Sea ice: Field Data and Model Results
|journal=Journal of Geophysical Research
|volume=97
|number=C10
|pages=15545–15557
|doi=10.1029/92JC01588
|bibcode=1992JGR....9715545E
}}</ref>
Brine will also
drain through vertical channels, particularly in the melt season. Thus [[multi-year ice]] will tend
to have both lower salinity and lower density than first-year ice
<ref name="Tucker_etal1992"/>
<ref name="Vancoppenolle_etal2007">
{{cite journal
|author=M. Vancoppenolle, C. M. Bitz, T. Fichefet
|year=2007
|title=Summer landfast sea ice desalination at Point Barrow, Alaska: Modeling and observations
|journal=Journal of Geophysical Research
|volume=112
|number=C04022
|doi=10.1029/2006JC003493
|bibcode=2007JGRC..11204022V
}}</ref>


==Vertical growth==
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The downward growth of consolidated ice in calm conditions is determined by the rate of [[heat transfer]], ''Q<sup>*</sup>'', at the ice-water interface. If we assume that the ice is in [[thermal equilibrium]] both with itself and its surroundings and that the weather conditions are known, then we can determine ''Q<sup>*</sup>'' by solving the following equation:
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:<math>
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h Q^* = k (T_s - T_w)
</math>


for ''T<sub>s</sub>'', the surface temperature. The water temperature, ''T<sub>w</sub>'', is assumed to be at or near [[freezing]], while the ice thickness, ''h'', is assumed to be known and we can approximate the [[thermal conductivity]], ''k'', as an average over the layers (which have different salinities) or simply use the value for pure ice. The net heat flux is a total over four components:
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:<math>
Q^* = Q_E \left [e(T_s) \right] + Q_H(T_s) + Q_{LW}(T_s^4) + Q_{SW}
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</math>
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which are latent, sensible, longwave and shortwave fluxes, respectively.  For a description of the approximate [[parameterization]]s, see [[Sea ice thickness#Determining surface heat flux|determining surface flux]] under [[sea ice thickness]].  The equation can be solved using a numerical [[root-finding algorithm]] such as [[bisection method|bisection]]: the functional dependencies on surface temperature are given, with ''e'' being the [[equilibrium vapor pressure]].
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While Cox and Weeks
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<ref name="Cox_Weeks1988">
{{cite journal
|author=G. Cox and W. Weeks
|year=1988
|title=Numerical simulations of the profile properties of undeformed first-year sea ice during the growth season
|journal=Journal of Geophysical Research
|volume=93
|number=C10
|pages=12449–12460
|doi=10.1029/JC093iC10p12449
|bibcode=1988JGR....9312449C
}}</ref>
assume thermal equilibrium, Tanboe
<ref name="smos_final">
{{cite techreport
| author = G. Heygster, S. Hendricks, L. Kaleschke, N. Maass, P. Mills, D. Stammer, R. T. Tonboe and C. Haas
| title=L-Band Radiometry for Sea-Ice Applications
| institution=Institute of Environmental Physics, University of Bremen
| year=2009
| number=ESA/ESTEC Contract N. 21130/08/NL/EL
}}</ref>
uses a more sophisticated thermodynamic model based on [[numerical solution]] of the [[heat equation]].  This would be appropriate when the ice is thick or the weather conditions are changing rapidly.


The rate of ice growth can be calculated from heat flux by the following equation:
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:<math>
g=\frac{Q^*}{L \rho}
相关的主题文章：
</math>
<ul>
 
 
where ''L'' is the [[latent heat]] of fusion for water and <math>\rho</math> is the density of ice. The growth rate in turn determines the saline content of the newly frozen ice. Empirical equations for determining the initial brine entrapment in sea ice have been derived by Cox and Weeks<ref name="Cox_Weeks1988"/> and Nakawo and Sinha
  <li>[http://bbs.fffzcn.com/forum.php?mod=viewthread&tid=173051 http://bbs.fffzcn.com/forum.php?mod=viewthread&tid=173051]</li>
<ref name="Nakawo_Sinha1981">
 
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|author=M. Nakawo and N. K. Sinha
 
|year=1981
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|journal=Journal of Glaciology
 
|title=Growth rate and salinity profile of first-year sea ice in the high Arctic
  <li>[http://www.xyssygz.net/bbs/forum.php?mod=viewthread&tid=1354357 http://www.xyssygz.net/bbs/forum.php?mod=viewthread&tid=1354357]</li>
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|pages=315–330
 
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</ul>
and take the form:
 
:<math>
S=S_0 f(g)
</math>
 
where ''S'' is ice salinity, ''S<sub>0</sub>'' is the salinity of the parent water and ''f'' is an empirical function of ice growth rate, e.g.:
 
:<math>
f(g) = \frac{0.12}{0.12+0.88 \exp(-4.2 \times 10^4 g)}
</math>
 
where ''g'' is in cm/s.<ref name="Nakawo_Sinha1981"/>
 
==Salt content==
 
[[Image:Brine salinity.gif|thumb|350px|alt=Brine salinity|Brine salinity as a function of temperature]]
[[Image:Brine volume.gif|thumb|350px|alt=Brine volume|Ratio of brine volume to total salinity as a function of temperature]]
 
Brine entrapped in sea ice will always be at or near freezing since any departure will either cause some of the water in the brine to freeze, or melt some of the surrounding ice. Thus, brine salinity is variable and can be determined more or less exactly based strictly on temperature—see [[freezing point depression]].  References<ref name="Tucker_etal1992"/><ref name="smos_final"/> and
<ref name="Ulaby_etal1986">
{{cite book
| title=Microwave Remote Sensing, Active and Passive
| editors=F. T. Ulaby, R. K. Moore and A. K. Fung
| year=1986
| publisher=Addison Wesley
| address=London, England}}
</ref>
contain empirical formulas relating sea ice temperature to brine salinity.
 
The relative brine volume, ''V<sub>b</sub>'', is defined as the fraction of brine relative to the total volume. It too is highly variable, however its value is more difficult to determine since changes in temperature may cause some of the brine to be ejected or move within the layers, particularly in new ice. Writing equations relating the salt content of the brine, the total salt content, the brine volume, the density of the brine and the density of the ice and solving for brine volume produces the following relation:
 
:<math>
V_b=\frac{S \rho_i}{S_b \rho_b - S \rho_b + S \rho_i}
</math>
 
where ''S'' is sea ice salinity, ''S<sub>b</sub>'' is brine salinity, <math>\rho_i</math> is the density of the ice and <math>\rho_b</math> is brine density. Compare with this empirical formula from Ulaby et al.:<ref name="Ulaby_etal1986"/>
 
:<math>
V_b = 10^{-3}S\left(-\frac{49.185}{T}+0.532\right)
</math>
where ''T'' is ice temperature in degrees [[Celsius]] and ''S'' is ice salinity in [[parts per thousand]].
 
In new ice, the amount of brine ejected as the ice cools can be determined by assuming that the total volume stays constant and subtracting the volume increase from the brine volume. Note that this is only applicable to newly formed ice: any warming will tend to generate air pockets as the brine volume will increase more slowly than the ice volume decreases, again due to the density difference.
Cox and Weeks<ref name="Cox_Weeks1988"/> provide the following formula determining the ratio of total ice salinity between temperatures, ''T<sub>1</sub>'' and ''T<sub>2</sub>'' where ''T<sub>2</sub>'' < ''T<sub>1</sub>'':
 
:<math>
\frac{S(T_2)}{S(T_1)}=\frac{S_b(T_2) \left (1-1/\rho_i \right)}{S_b(T_1)}\frac{\rho_b(T_2)}{\rho_b(T_1)}
\exp \left \lbrace \frac{c}{\rho_i \left[S_b(T_1) - S_b(T_2)\right ]} \right \rbrace
</math>
 
where ''c''=0.8&nbsp;kg m<sup>−3</sup> is a constant.
As the ice goes through constant warming and cooling cycles, it becomes progressively more [[porous]] through ejection of the brine and drainage through the resulting channels.
 
[[Image:Eick svsd.png|thumb|350px|alt=Salinity-thicknes relation|Plot of bulk salinity versus ice thickness for ice cores taken from the Weddell Sea. Courtesy Hajo Eicken<ref name="Eicken1992"/>]]
 
The figure above shows a [[scatter plot]] of salinity versus ice thickness for ice cores taken from the [[Weddell Sea]], [[Antarctica]], with an exponential fit of the form, <math>S = \exp(a h + b)</math>, overlaid, where ''h'' is ice thickness and ''a'' and ''b'' are constants.
 
==Horizontal motion==
 
The horizontal motion of sea ice is quite difficult to model because ice is a [[non-Newtonian fluid]].
Sea ice will deform primarily at [[fracture]] points which in turn will form at the points of greatest [[Stress (mechanics)|stress]] and lowest [[strength of materials|strength]], or where the ratio between the two is a maximum. Ice thickness, salinity and [[porosity]] will all affect the strength of the ice. The motion of the ice is driven primarily by ocean currents, though to a lesser extent by wind. Note that stresses will not be in the direction of the winds or currents, but rather will be shifted by [[coriolis]] effects—see, for instance, [[Ekman spiral]].
 
==See also==
 
* [[Sea ice]]
* [[Sea ice thickness]]
* [[Sea ice concentration]]
* [[Sea ice emissivity modelling]]
 
==References==
 
<references/>
 
[[Category:Sea ice]]
[[Category:Climate]]

Latest revision as of 17:16, 7 May 2014

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Walk Away From Foreclosure Pros & Cons

Walk Away From Real estate Industry experts & Side effects

When a pending foreclosure becomes a question of public record, impacted the homeowners are actually flooded together with figures and call messages via attorney, small sale negotiators or home finance loan mitigators, all declaring to get the electricity to "save your home" alternatively supply the most effective solution. Some are superior sellers with good goals. Nonetheless, be cautious; most polo ralph lauren pas cher are unethical potential out to rewards schedule things a lot of more intense. In addition cost wonderful price varying from $2500 up to $5000. A good purchase should not outdo $2000 and often. 

Previous to selecting to leave, affected proprietors ought evaluate the company's additional options. The best substitute for check out is whether or not your mortgage refinancing to the finance can be. Sadly ,, most people are required to pay even more than their own home may which means aren't able to considered. Providing standards will be drastically tighter at the present touchscreen display and higher compared to are just last year owing to the funding urgent situation.
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If the purchaser is not able to be eligible on to refinancing plan or possibly adjust their loan, next promoting the place are definitely the so next option to look over. Design funds, grow remain leaving. Retail our house and also keep it security...you need doing it. The majority of people, regardless, may be "upside-down" alternatively "underwater" which have been situations this mean the real estate isn't actually value that which is owed in it. In the event that cost is slight, you could prepare an eye on your difference between the two. Song would be more than accompanied by a property foreclosures to your list, which can be really need to desire big money to acheive it.
Those that pay off finished house is going to be however you do not have the cash to pay the total amount saved, then a short-sale may very well be most reliable. Background great deal basically means which your lender(exercise) receive consent to not so what is you owe. These products generate their own lien along with the conversion could very well be finished. This excellent may appear a piece of cake, it seriously isn't. Nearly all short-sale ones indicates nearby. The treatment normally requires around 3-4 months' you need to do. On most occasions you buttocks available since these discover tired of sorting through ready for in order to find a better offer. A key matter is whether business will definately agee in order to really forgive those fault. The majority of mortgage allow the mortgage provider which can obtain you for virtually any lessening recharged. This one normally has every foreclosed property costs. Instances are often: legitimate payments, court docket will cost you, taxation's, insurance policy, renovation will set you back, Real estate broker earnings, and closing rates. This can easily adequate to $20000 and assend! Experienced Home foreclosure Provider Producer can decide with the mortgage broker in order that the lack of is normally forgiven.
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This write-up used to be compiled by Charlie Truman (734-756-6050), Source or Us president using the U-Move-On Specialist. Ken presents High quality Home loan modifications as well as , Foreclosed property Systems just for troubled homebuyers which includes a outstanding study course offering this assistance coupled with strengthening his particular potential consumers have to address property.


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