Steven Dutch, Professor Emeritus, Natural and Applied Sciences, Universityof Wisconsin - Green Bay
The Phase Rule is P + F = C + 2, where
The familiar systems below illustrate the phase rule. In both cases, C = 1 so P + F = C+ 2 = 3.
The phase rule applies only to chemical systems in equilibrium. It plays very littlerole in sedimentary petrology, where rocks consist of diagenetic minerals that may be inequilibrium, but also detrital minerals that may be wildly out of equilibrium. It may playa role at times in igneous petrology, but igneous rocks are often non-equilibrium becausecrystals may be zoned or rimmed and their interiors isolated from the rest of the magma.The phase rule figures prominently in metamorphic petrology, where equilibrium is commonlythe rule.
What constitutes a component is sometimes a matter of definition, for example, if acomponent is always present, we may simply ignore it. If a rock contains Al2SiO5 andquartz, we might choose to ignore the quartz, if it doesn't participate in any chemicalreactions. Or we might choose to count quartz as a phase, in which case we must also countSiO2 as a component. We don't need to consider Al2O3 and SiO2 as separate components ifthey always occur as Al2SiO5. However, if there were the possibility that quartz orcorundum might occur as well, then we would have to consider Al2O3 and SiO2 as separatecomponents.
Most of the time F = 2; temperature and pressure. Occasionally F can be greater, forexample if total pressure and water pressure are different, or if the relative pressuresof water and carbon dioxide are important, or if oxidation potential is important.
If F = 2 then P + 2 = C + 2 and P = C.
We see this to some extent in calculating norms for igneous rocks; titanium is assumed togo into titanite or ilmenite, phosphorus into apatite, and so on. For each component,there is a phase.
In metamorphic rocks, we need to consider these important components: SiO2, Al2O3, FeO,Fe2O3, CaO, Na2O, K2O, MgO, TiO2 and H2O. The most components we can conveniently dealwith at one time is only three, on a triangle plot. Ten components, taken in threes, makesfor (10*9*8)/(1*2*3) = 120 triangle plots. Nobody has ever plotted phase diagrams in that sort of detail.
We can simplify by making certain simplifying assumptions:
Thus we simplify to the following components: (SiO2), (Al2O3), (FeO + MgO), CaO, Na2O,and K2O. Thus C = 6, which means (if F = 2) that P = 6. Most metamorphic rocks typicallycontain 5 or 6 main mineral phases. Minor components like Cr, or P usually have their ownphases (chromite and apatite, respectively).
With a few further simplifying assumptions, we can reduce C to 3 and plot thesystems on triangle plots. Among the most common assumptions:
By applying these simplifying assumptions appropriately, we can describe manymetamorphic rocks in terms of three variable components (which we're interested in) andthree background components that are always accounted for in certain ways (which weignore).
In the ACF diagram, we assume K always goes into feldspar or mica, Na into albite, andquartz is present. That leaves Al, Ca and Fe-Mg to account for. We define:
In the A'KF diagram, we track Al, K and Fe-Mg. We define:
This diagram is often paired with the ACF diagram, and all the minerals on the A'-Fedge plot in the same places. Thus, many references show this diagram point-down.
Phengite is muscovite with substantial Mg and Fe, stable at low temperatures and highpressures.
This diagram attempts to deal with the fact that Fe and Mg do not fully substitute forone another. Many of the ferromagnesian minerals also contain Al, but biotite alsocontains K. Thus, we have to track four components in a tetrahedron. We do this byassuming that muscovite is always present in these rocks, picking the muscovite point asour projection point, then projecting everything onto the AFM plane. Note that some pointsplot inside the AFM triangle and some outside.
|In this diagram, composition a plots at a' inside the Al-Mg-Fe triangle but b plots at b', outside it. |
K-feldspar is usually said to plot at infinity on this plot but in reality it never plots on the AFM plane at all.
|Principal minerals tracked on this plot are shown here. Al2O3 is usually occupied by pyrophyllite, andalusite, kyanite or sillimanite. |
Mg-Fe silicates like olivine, enstatite-hypersthene, anthophyllite, and so on would plot along the Mg-Fe line but this diagram is almost never used for rocks where these minerals would occur.
Virtually every text describes and uses this diagram wrong! Mineralassemblages, as in all other phase diagrams, are indicated with tie lines joiningcoexisting minerals. Since all of these minerals have very variable compositions, thediagrams are typically shown with fanning bundles of tie lines connecting the range ofcompositions of one mineral with that of another. It's either said or implied that the tieline joins the composition of one mineral to the corresponding composition of the other.
A little thought will suffice to show that this is almost never true. For one thing,there simply isn't enough compositional data in many cases to support such a claim. Ifsuch data did exist, the tie lines would have to be precisely plotted based on actual dataand would be identical from diagram to diagram. They never are. For another, as therelative amounts of Fe, Mg and Al vary, tie lines can never sort out cleanly - tie linesjoining say, stilpnomelane, biotite and chlorite in one rock will almost certainly crosstie lines to these minerals in other, slightly different rocks.
Rather than continue the misleading tradition of tie line bundles, which is visuallycluttered and geologically meaningless anyway, it seems far more preferable simply to drawa single tie line from the average composition of one phase to the average of any otherphase.
This is the standard diagram for dealing with carbonate rocks.
Since P + F = C + 2, and C = 3, then P + F for a standard metamorphic triangle plot isequal to 5. Normally, in any stability field of a phase diagram, 3 phases are present andthere are 2 degrees of freedom, usually temperature and pressure. When a reaction is atequilibrium, we are on some T-P reaction curve and the number of degrees of freedom dropsto one. (If we vary temperature, we also have to vary pressure to stay on the T-P reactioncurve. If we depart from the reaction curve at all, the chemical reaction will run in onedirection or the other to completion.) Thus, while a reaction is in progress, F = 1 and P= 4. We can have 4 phases present in one of several ways:
The low-temperature metamorphism of carbonate rocks illustrates these possible changes:
The left-hand diagram shows the normal carbonate sedimentary assemblage. the phasesrepresented are quartz (Q), calcite (C), dolomite (D) and magnesite (M). Around 400 C,talc forms via the reaction 3Mag + 4Qz + H2O = Tc + 3CO2. The newpoint representing talc (red) forms along the Q-M side of the triangle (center). As thereaction runs to completion, quartz and magnesite become incompatible and a new tie lineforms between talc and dolomite (right). Note that dolomite does not participate in thereaction at all.
Around 450 C, dolomite ceases to coexist with quartz and the reaction
3Dol + 4Qz + H2O = Tc + 3Cal + 3CO2 occurs. The Q-D tie linedisappears (center) and there are 4 phases present at equilibrium. As the reaction runs tocompletion a new tie line joining talc and calcite appears (red, right). Note that thedissolved tie line joins the reactants and the new tie line joins the products.
Around 500 C, quartz, calcite and talc react to form tremolite. The new tremolite pointappears in the middle of the Q-Tc-C field (center) and as the reaction runs to completion,new tie lines joining tremolite with quartz, talc and calcite appear (right).
At slightly higher temperatures talc and calcite react. The talc-calcite tie linedisappears and at equilibrium there are four phases present (center). As the reaction runsto completion a new tie line joining tremolite and and dolomite appear (red, right).
Created December 1, 1997, Last Update 31 May 2020
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