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Ice sheets, of which the West Antartic, East Antarctic, and Greenland ice sheets are the only current examples, are basically like very large domes of ice, on t

Ice sheets, of which the West Antartic, East Antarctic, and Greenland ice sheets are the only current examples, are basically like very large domes of ice, on the order of 1000 kilometers wide and 1-3 kilometers high. Unlike mountain glaciers, they completely cover the underlying topography. They flow outwards under their own weight into the ocean. In Antarctica, it is cold enough that melting at the surface is negligible. This means that almost all snow that falls ultimately must flow into the ocean. At some point at the edge, the ice loses contact with the ground and floats. This is the grounding line. For a constant ice flow velocity, the amount of ice that gets spit out into the ocean is proportional to how thick the ice is at the grounding line. Now, suppose that the slope of the bed gets deeper as you go from the grounding line into the interior of the ice sheet. Then, if the grounding line retreats, it's in deeper water. So, the ice flux increases. The increasing ice flux means that the ice sheet thins near the edge. Since it's thinner, it can't stay grounded in as deep of water. Imagine a big chunk of ice in a puddle of water that sits at the bottom of a puddle, versus a little piece that floats. Now, since it can't float in as deep of water, the grounding line retreats because bouyancy is pulling up on the edge. This makes it go into deeper water, ice flux increases more, etc. This could cause a collapse of the ice sheet, resulting in a few meters of rise. The timescale that this could happen is very poorly constrained (decades? centuries? a couple millenia?). It may have already irreversibly begun, or maybe not.

function_seven 8y ago
I still had trouble visualizing what you're describing. This is a typical cross-section[1]. To make it match what you're describing, I'd draw a slope from the grounding line and downward to the left, right? (Image depicts a flat bed underneath the ice, instead of a slope downward as you go inward) [1] http://cdn.antarcticglaciers.org/wp-content/uploads/2014/09/Fig-2.-Grounding-line.png http://cdn.antarcticglaciers.org/wp-content/uploads/2014/09/... EDIT: I think this image is a better representation: http://cdn.antarcticglaciers.org/wp-content/uploads/2014/05/PIG.ai_.jpg http://cdn.antarcticglaciers.org/wp-content/uploads/2014/05/...
- dsfyu404ed 8y ago
  Flip the terrain illustration in that picture left to right and make it steeper. The terrain that this particular glacier is a bowl that is well below sea level. The more the glacier retreats the deeper the water gets (because the terrain is deeper), the more of the glacier can be floated, the faster the glacier can melt. Imagine a pool that slopes from 3ft to 8ft full of ice melting. The thin part melts first, lifts up, water gets a little further underneath lifting the next bit of ice and melting it faster but because the pool gets deeper as you go the more ice can be lifted up and broken off so it melts faster as it goes. Edit: yes, your second image is spot on.
  - deleted 8y ago
    [deleted]
  - Gibbon1 8y ago
    First image alludes to something. Near freezing slightly warmer water is denser. So convection is reversed. Unless I'm mistaken.
    - function_seven 8y ago
      Both images show that convection pattern, but only the second image illustrates what parent was referring to, with the ground level dropping inward. As the groundline recedes, the surface area of ice exposed to the water increases, resulting in a positive feedback loop and further accelerating the melt rate.
    - lenticular 8y ago
      That's right. Water is most dense at about 4 degrees, and lower in sea water (around 1 C I believe). Below that, and water molecules start forming ephemeral crystal lattices. Since, weirdly, the hexagonal structure of ice lattices takes up more room than in liquid form, this makes the water less dense. Just to be clear, it isn't actually crystallizing at these temperatures, but due to fluctuations, crystal lattices can be briefly formed.
NPMaxwell 8y ago
The "few meters of rise" you mention are meters of rise of global sea levels?
- btilly 8y ago
  Yup. Per https://en.wikipedia.org/wiki/West_Antarctic_Ice_Sheet#Potential_collapse https://en.wikipedia.org/wiki/West_Antarctic_Ice_Sheet#Poten... the potential rise is 4.8 meters, which is 16 feet. Of course a likely collapse will be some fraction of that. Unfortunately there are big question marks about how quickly it could happen. But we do get very large icebergs every so often - for example a couple of years ago there was one the size of Delaware. (Of course floating ice to floating freely moving ice does not directly change sea level. It does make sea water a bit fresher though.)
mikestew 8y ago
I'll admit that I'm still a little lost, but thank you for going out of your way to try and explain it. It's not your explanation, it's me. :-) EDIT: thanks, function_seven; pictures help the five-year old in all of us.
irrational 8y ago
>Now, suppose that the slope of the bed gets deeper as you go from the grounding line into the interior of the ice sheet. Then, if the grounding line retreats, it's in deeper water. So, the ice flux increases. The increasing ice flux means that the ice sheet thins near the edge. Since it's thinner, it can't stay grounded in as deep of water. This is where you lost me. Bed? Flux? Can you explain what this paragraph means like I'm 5?
- kaybe 8y ago
  The bed is the ground below the glacier. In this case, it is below the sea level. The glacier is thick, so there are parts where it is not floating, but actually lying on the sea floor. (You can probably imagine what happens if you put a lot of ice in a shallow pool.) Because the glacier is thick (non-Newtonian fluid btw! this means it will change it's 'liquidity' if you put stress on it.) it will flow outward. At some point it will be thin enough and/or the sea floor deep enough that it can float on the sea water. The place where that happens is important, because floating ice displaces water, so it will not raise the sea level anymore if it melts (which is why we're not too worried about the Arctic ice melting, at least with concern to sea level rise). This place, or rather line since it is a 3D glacier, is the grounding line. In general, flux is the amount of something flowing through a set point or line. (e.g. If you stand next to a river, the flux is the total amount of water passing you in, say, a minute.) In this case, we watch the flow of ice through the grounding line. The velocity of it should be constant, so the same speed always, because the ice is flowing from the center and is pushing constantly. This means that if the ice is thicker there, you get more flow because a higher amount of ice can pass at the same time. (Imagine a river with the same water speed but twice the depth - more water passing by.) The ice flowing into the sea breaks of or melts and is thus lost to the glacier. So if the grounding line is in deeper water, there will be more ice mass lost over the same time period. Normally you'd expect the sea to get deeper the farther you get away from the glacier. In some cases, and quite often in West Antarctica, this is actually not the case. The further you get 'inland', the deeper the sea gets. (Still covered fully in ice that is lying on the sea floor/bed.) This is an unstable situation. When more ice is lost at the front due to melting etc, and the place where the glacier still lies on the sea floor (grounding line) retreats a little, at this place the glacier will now be thicker than before (same height at the top + lower ground = 'deeper river'). The ice speed stays the same, so now we lose more ice at the grounding line. This makes the ice thinner at the edge (because more ice is lost than before). If it gets thinner it can float more easily, and the grounding line goes back a little. This is a run-away process until we reach an area where the sea does not get deeper anymore. Does this help?

function_seven 8y ago

I still had trouble visualizing what you're describing. This is a typical cross-section[1]. To make it match what you're describing, I'd draw a slope from the grounding line and downward to the left, right? (Image depicts a flat bed underneath the ice, instead of a slope downward as you go inward) [1] http://cdn.antarcticglaciers.org/wp-content/uploads/2014/09/Fig-2.-Grounding-line.png http://cdn.antarcticglaciers.org/wp-content/uploads/2014/09/... EDIT: I think this image is a better representation: http://cdn.antarcticglaciers.org/wp-content/uploads/2014/05/PIG.ai_.jpg http://cdn.antarcticglaciers.org/wp-content/uploads/2014/05/...

dsfyu404ed 8y ago
Flip the terrain illustration in that picture left to right and make it steeper. The terrain that this particular glacier is a bowl that is well below sea level. The more the glacier retreats the deeper the water gets (because the terrain is deeper), the more of the glacier can be floated, the faster the glacier can melt. Imagine a pool that slopes from 3ft to 8ft full of ice melting. The thin part melts first, lifts up, water gets a little further underneath lifting the next bit of ice and melting it faster but because the pool gets deeper as you go the more ice can be lifted up and broken off so it melts faster as it goes. Edit: yes, your second image is spot on.
- deleted 8y ago
  [deleted]
- Gibbon1 8y ago
  First image alludes to something. Near freezing slightly warmer water is denser. So convection is reversed. Unless I'm mistaken.
  - function_seven 8y ago
    Both images show that convection pattern, but only the second image illustrates what parent was referring to, with the ground level dropping inward. As the groundline recedes, the surface area of ice exposed to the water increases, resulting in a positive feedback loop and further accelerating the melt rate.
  - lenticular 8y ago
    That's right. Water is most dense at about 4 degrees, and lower in sea water (around 1 C I believe). Below that, and water molecules start forming ephemeral crystal lattices. Since, weirdly, the hexagonal structure of ice lattices takes up more room than in liquid form, this makes the water less dense. Just to be clear, it isn't actually crystallizing at these temperatures, but due to fluctuations, crystal lattices can be briefly formed.

NPMaxwell 8y ago

The "few meters of rise" you mention are meters of rise of global sea levels?

btilly 8y ago
Yup. Per https://en.wikipedia.org/wiki/West_Antarctic_Ice_Sheet#Potential_collapse https://en.wikipedia.org/wiki/West_Antarctic_Ice_Sheet#Poten... the potential rise is 4.8 meters, which is 16 feet. Of course a likely collapse will be some fraction of that. Unfortunately there are big question marks about how quickly it could happen. But we do get very large icebergs every so often - for example a couple of years ago there was one the size of Delaware. (Of course floating ice to floating freely moving ice does not directly change sea level. It does make sea water a bit fresher though.)

mikestew 8y ago

I'll admit that I'm still a little lost, but thank you for going out of your way to try and explain it. It's not your explanation, it's me. :-) EDIT: thanks, function_seven; pictures help the five-year old in all of us.

irrational 8y ago

>Now, suppose that the slope of the bed gets deeper as you go from the grounding line into the interior of the ice sheet. Then, if the grounding line retreats, it's in deeper water. So, the ice flux increases. The increasing ice flux means that the ice sheet thins near the edge. Since it's thinner, it can't stay grounded in as deep of water. This is where you lost me. Bed? Flux? Can you explain what this paragraph means like I'm 5?

kaybe 8y ago
The bed is the ground below the glacier. In this case, it is below the sea level. The glacier is thick, so there are parts where it is not floating, but actually lying on the sea floor. (You can probably imagine what happens if you put a lot of ice in a shallow pool.) Because the glacier is thick (non-Newtonian fluid btw! this means it will change it's 'liquidity' if you put stress on it.) it will flow outward. At some point it will be thin enough and/or the sea floor deep enough that it can float on the sea water. The place where that happens is important, because floating ice displaces water, so it will not raise the sea level anymore if it melts (which is why we're not too worried about the Arctic ice melting, at least with concern to sea level rise). This place, or rather line since it is a 3D glacier, is the grounding line. In general, flux is the amount of something flowing through a set point or line. (e.g. If you stand next to a river, the flux is the total amount of water passing you in, say, a minute.) In this case, we watch the flow of ice through the grounding line. The velocity of it should be constant, so the same speed always, because the ice is flowing from the center and is pushing constantly. This means that if the ice is thicker there, you get more flow because a higher amount of ice can pass at the same time. (Imagine a river with the same water speed but twice the depth - more water passing by.) The ice flowing into the sea breaks of or melts and is thus lost to the glacier. So if the grounding line is in deeper water, there will be more ice mass lost over the same time period. Normally you'd expect the sea to get deeper the farther you get away from the glacier. In some cases, and quite often in West Antarctica, this is actually not the case. The further you get 'inland', the deeper the sea gets. (Still covered fully in ice that is lying on the sea floor/bed.) This is an unstable situation. When more ice is lost at the front due to melting etc, and the place where the glacier still lies on the sea floor (grounding line) retreats a little, at this place the glacier will now be thicker than before (same height at the top + lower ground = 'deeper river'). The ice speed stays the same, so now we lose more ice at the grounding line. This makes the ice thinner at the edge (because more ice is lost than before). If it gets thinner it can float more easily, and the grounding line goes back a little. This is a run-away process until we reach an area where the sea does not get deeper anymore. Does this help?