<p>This answer is based on Winter's presentation for his textbook. Look up chapter 7 on his <a href="https://www.whitman.edu/geology/winter/JDW_PetClass.htm" rel="nofollow noreferrer">website</a>, and start at slide 39.</p>

<p>First let's go through some of your statements:</p>

<blockquote>
  <p>Felsic magmas crystallise in the crust, unlike mafic magmas which tend to make it to the Earth's surface</p>
</blockquote>

<p>Not necessarily. It is true the upper continental crust is composed mostly of felsic intrusive magmas, everything else is not. The lower continental crust, the oceanic crust, arcs, etc., those are all mostly mafic. </p>

<blockquote>
  <p>They are more viscous than mafic magmas and therefore it is mechanically harder to ascend</p>
</blockquote>

<p>This only means they ascend slower than mafic magmas. Eventually it all depends on buoyancy. If they're liquid and less dense than the surrounding rocks, they go up.</p>

<blockquote>
  <p>They are colder, so crystallise earlier, so travel less distance</p>
</blockquote>

<p>Not necessarily. Their final crystallisation temperatures (aka "solidus") are also lower than mafic magmas. That's why they are liquid at temperatures that mafic melts would already be solid. This has little implication to the distance they travel (to a first order approximation).</p>

<blockquote>
  <p>They are more hydrous than mafic magmas...</p>
</blockquote>

<p>True! The reasons for why felsic magmas are (generally) more hydrous than mafic magmas are not important now.</p>

<blockquote>
  <p>why does losing water encourage felsic magma to crystallise in the crust? Is it something to do with water being a network modifier?</p>
</blockquote>

<p>Yes. Water, or more precisely, H<sub>2</sub>O acts as a flux: it is a chemical component that strongly lowers the melting temperatures of various materials, including rocks. It follows the basic chemical reaction of $\ce{rock + H2O = melt-with-H2O-dissolved-in-it}$.</p>

<p>The important part is that to allow H<sub>2</sub>O to be dissolved in the melt, you need to have some pressure. Otherwise the H<sub>2</sub>O just exsolves out and leaves the magma, similar to opening a bottle of carbonated drink (think coke). While there is pressure, the CO<sub>2</sub> is in the drink. When you open the cap and depressurise it, the CO<sub>2</sub> comes out of the drink.</p>

<p>Something similar happens in magmas. You have a felsic magma with H<sub>2</sub>O dissolved in it (otherwise it wouldn't be liquid, it would be solid) rising upwards through the crust. Because it goes up, the pressure around it goes down, causing H<sub>2</sub>O to leave the magma as bubbles of water vapour (or a supercritical fluid, depending on depth). Then, as the magma loses the flux, it solidifies before it can even reach the surface. Here's a diagram to explain this, in the albite-H<sub>2</sub>O simplified system, which is a good model for granites and felsic magmas:</p>

<p><a href="https://i.sstatic.net/Yw0g3.jpg" rel="nofollow noreferrer"><img src="https://i.sstatic.net/Yw0g3.jpg" alt="enter image description here"></a></p>

<p>At surface pressure (bottom of the diagram) albite melts at slightly above 1100 °C. In a dry system, the higher the pressure, the higher the temperature. For example, at 5 kbar (0.5 GPa) the melting point of albite goes up to 1200 °C. If you add H<sub>2</sub>O at surface pressures, it doesn't change anything because there is not enough pressure to put the H<sub>2</sub>O in the (non-existing) melt. But at higher pressure it is possible for H<sub>2</sub>O to dissolve in the melt, thus allowing the existence of melt. For example at 5 kbar the melting point of albite with more than enough (aka saturated) H<sub>2</sub>O goes down to 800 °C. That's 400 °C below the dry melting point!</p>

<p>So what would happen if a melt containing some H<sub>2</sub>O starts rising upwards at constant temperature? For example at point a to d in the diagram. It will lose H<sub>2</sub>O as it rises, increasing the solidus temperature. Because the magma is not hot enough to be liquid at the surface, it will freeze before that, while still at depth.</p>

CC BY-SA 3.0
2017-04-30T08:08:59.557Z
2017-04-30T08:08:59.557Z
Gimelist
<p>Felsic magmas crystallise in the crust, unlike mafic magmas which tend to make it to the Earth's surface, for the following reasons:</p>

<ol>
<li>They are more viscous than mafic magmas and therefore it is mechanically harder to ascend,</li>
<li>They are colder, so crystallise earlier, so travel less distance,</li>
<li>They are more hydrous than mafic magmas and the loss of water encourages crystallisation .</li>
</ol>

<p>My question is, why does losing water encourage felsic magma to crystallise in the crust? Is it something to do with water being a network modifier?</p>

CC BY-SA 3.0
2017-04-29T12:05:47.643Z
Most mafic magmas also crystallise in the crust. In terms of volume of melt, plutonism is far more important than volcanism, for both mafic and felsic melts.
bon
<water><crust><magmatism><igneous>
Why does the loss of water from a felsic magma encourage crystallisation?
Kate
# Why does the loss of water from a felsic magma encourage crystallisation?

(Asked by: username_0 on 2017-04-29)

Felsic magmas crystallise in the crust, unlike mafic magmas which tend to make it to the Earth's surface, for the following reasons:

1. They are more viscous than mafic magmas and therefore it is mechanically harder to ascend,
2. They are colder, so crystallise earlier, so travel less distance,
3. They are more hydrous than mafic magmas and the loss of water encourages crystallisation .

My question is, why does losing water encourage felsic magma to crystallise in the crust? Is it something to do with water being a network modifier?

**Tags:** water, crust, magmatism, igneous

> **Comments:**
> **username_1**: Most mafic magmas also crystallise in the crust. In terms of volume of melt, plutonism is far more important than volcanism, for both mafic and felsic melts.  

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## 1 answers

### Answer by username_2 on 2017-04-30. Score: 2

This answer is based on Winter's presentation for his textbook. Look up chapter 7 on his [website](https://www.whitman.edu/geology/winter/JDW_PetClass.htm), and start at slide 39.

First let's go through some of your statements:

> Felsic magmas crystallise in the crust, unlike mafic magmas which tend to make it to the Earth's surface

Not necessarily. It is true the upper continental crust is composed mostly of felsic intrusive magmas, everything else is not. The lower continental crust, the oceanic crust, arcs, etc., those are all mostly mafic.

> They are more viscous than mafic magmas and therefore it is mechanically harder to ascend

This only means they ascend slower than mafic magmas. Eventually it all depends on buoyancy. If they're liquid and less dense than the surrounding rocks, they go up.

> They are colder, so crystallise earlier, so travel less distance

Not necessarily. Their final crystallisation temperatures (aka "solidus") are also lower than mafic magmas. That's why they are liquid at temperatures that mafic melts would already be solid. This has little implication to the distance they travel (to a first order approximation).

> They are more hydrous than mafic magmas...

True! The reasons for why felsic magmas are (generally) more hydrous than mafic magmas are not important now.

> why does losing water encourage felsic magma to crystallise in the crust? Is it something to do with water being a network modifier?

Yes. Water, or more precisely, H2O acts as a flux: it is a chemical component that strongly lowers the melting temperatures of various materials, including rocks. It follows the basic chemical reaction of $\ce{rock + H2O = melt-with-H2O-dissolved-in-it}$.

The important part is that to allow H2O to be dissolved in the melt, you need to have some pressure. Otherwise the H2O just exsolves out and leaves the magma, similar to opening a bottle of carbonated drink (think coke). While there is pressure, the CO2 is in the drink. When you open the cap and depressurise it, the CO2 comes out of the drink.

Something similar happens in magmas. You have a felsic magma with H2O dissolved in it (otherwise it wouldn't be liquid, it would be solid) rising upwards through the crust. Because it goes up, the pressure around it goes down, causing H2O to leave the magma as bubbles of water vapour (or a supercritical fluid, depending on depth). Then, as the magma loses the flux, it solidifies before it can even reach the surface. Here's a diagram to explain this, in the albite-H2O simplified system, which is a good model for granites and felsic magmas:

[![enter image description here](https://i.sstatic.net/Yw0g3.jpg)](https://i.sstatic.net/Yw0g3.jpg)

At surface pressure (bottom of the diagram) albite melts at slightly above 1100 °C. In a dry system, the higher the pressure, the higher the temperature. For example, at 5 kbar (0.5 GPa) the melting point of albite goes up to 1200 °C. If you add H2O at surface pressures, it doesn't change anything because there is not enough pressure to put the H2O in the (non-existing) melt. But at higher pressure it is possible for H2O to dissolve in the melt, thus allowing the existence of melt. For example at 5 kbar the melting point of albite with more than enough (aka saturated) H2O goes down to 800 °C. That's 400 °C below the dry melting point!

So what would happen if a melt containing some H2O starts rising upwards at constant temperature? For example at point a to d in the diagram. It will lose H2O as it rises, increasing the solidus temperature. Because the magma is not hot enough to be liquid at the surface, it will freeze before that, while still at depth.


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