**Equations of State (EOS)**

by Sylvia-Monique Thomas, University of Nevada Las Vegas

**Outline**

**Introduction**

**What is an Equation of State (EoS)?**

An EoS is the relation between functions of state, such as temperature (T), pressure (P), volume (V), internal energy or specific heat. It characterizes the state of matter of a material under a given set of physical conditions. EoSs are used to describe gases, fluids, fluid mixtures and solids. In mineral physics an EoS is used to determine mineral composition at depth (i.e., P and T) and depicts how the volume or equivalently density of a material vary as a function of depth, i.e., as a function of P and T. It reflects atomic structure, chemical bonding and stability of a material.

**Types of Equations of State**

The simplest equation of state is the one for ideal gases:

PV = nRT

where n is the number of moles and R is a constant, the gas constant R = 8.31451 J K^{-1} mol^{-1}. For a volume of ideal gas (V) experiencing an external pressure (P), there will be a related increase in temperature of the gas given by PV / R.

However, at high pressure and at low temperature, real gases deviate from the ideal gas law and the equation needs to be modified.

The EoS for solids and liquids also needs to be modified, more complex EoSs are necessary and various equations have been proposed, which will be discussed below.

For most solids and liquids, the effect of pressure is much greater than the effect of temperature, over the range of temperatures and pressures relevant to the Earth. Therefore it is easier to consider initially an isothermal EOS and then introduce a thermal expansion coefficient as temperature correction.

All EoS are based on assumptions. They are tested by their ability to reproduce the experimental data. Here we will focus on the most commonly used equations. We will start by examining the effect of pressure, i.e. the isothermal EoS.

**Isothermal Equation of State**

The simplest **isothermal** EoS for a solid is the bulk modulus or incompressibility, K:

K = -V (∂P/∂V)

where *∂*P/*∂*V is the partial derivative of pressure with respect to volume. The bulk modulus is a measure of the ability of a material to withstand changes in volume when under uniform compression.

This equation is only valid for a constant K or at P < K, because with increasing P a material's bulk modulus increases, the material becomes stiffer, hence a new formulation is required for a **linearly increasing K**:

K = K_{0}+ K_{0}' P

where K_{0} is the bulk modulus at room pressure and **K _{0}'=(**

**∂**

**K/**

**∂**

**P)**is the pressure derivative of K, which is assumed to be pressure-dependent.

_{P=0}After integration this leads to the Murnaghan EoS.

1)Murnaghan - 1937

The Murnaghan EoS can be derived from the assumption that the **bulk modulus varies linearly with pressure**, which results in:

V = V_{0}(1+K'P/ K_{0})

This EoS is widely used and known to reproduce both, P-V data and the correct values of the room pressure bulk modulus for compressions up to about 10%.

2) Birch-Murnaghan - 1947

The Birch-Murnaghan EoS (BMEOS) is the most widely used EoS by mineralogists. It's based on the Eulerian strain (

*f*):

_{E}In the 2^{nd} order BMEOS K_{0}' is set to a fixed value of 4. The 3^{rd} order BMEOS is used at very high pressures where *D*K/*D*P varies significantly with pressure. It is a 3-parameter EoS (V_{0}, K_{0} and K'') with f_{E}^{2} = 0 and

In the 4

^{th}order BMEOS K'' varies as function of pressure, and can be used for extremely condensed materials.

3)Natural strain EoS / Poirier and Tarantola – 1998

It's a logarithmic EoS, based on the 'Hencky' measure of linear strain or 'natural' strain (*f _{N}*).

In contrast to the 2^{nd} order BMEOS here K' = 2 at second order. In the 3^{rd} order EoS K'' is usually much larger than K'' in the 3^{rd} oder BMEOS:

.

4)Vinet EoS / 'Universal EoS' – 1986

It is used for solids at very high pressure and and is based on the Vinet strain (*f _{V}*). It corrects finite-strain EoS, such as the BMEOS, by incorporating volume variation of solids under high-pressure conditions.

with K' = 1 and

.

**Thermal Equation of State**

The simplest isobaric EOS for a solid is just the definition for the thermal expansion coefficient, a.

A thermal EoS describes a material's reaction to temperature changes. When a material is heated, the thermal pressure in the system changes and results in thermal expansion. One example of EoS used for high-temperature (up to 1000 K) and high-pressure data is the high-temperature BMEOS.

1)High-temperature Birch-Murnaghan EoS

Thermal expansion coefficient and bulk modulus are assumed to vary linearly with temperature,

,

where T_{0} is the reference temperature (298 K).

**Techniques**

1) Experimental Determination of an Equation of State

P-V-T data are experimentally determined utilizing a variety of shock compression, multi-anvil or diamond anvil cell experiments in combination with diffraction techniques.

2) Data Analysis: Least-squares fitting

EoS parameters are best estimated using least-squares fitting with pressure usually chosen as the dependent variable, P = f(V,T). The choices of which parameters to refine and which parameters to fix are critical for final fit values and their interpretation. Details about refinement strategy can be found in [2].

3) Data Analysis: Visual quality assessment

_{0}and K'. In addition, the slope is used to infer the correlation of the calculated variables. Here, the negative slope indicates the strong negative correlation of K

_{0}and K'.

*High-temperature and high-pressure crystal chemistry*, Reviews in Mineralogy and Geochemistry, 41, 35-60. Copyright © 1997 - 2012 Mineralogical Society of America. All rights reserved

**Confidence ellipses**

_{0}and K'. The correlation coefficient indicates if two parameters, such as in this case K

_{0}and K', are independent or dependent of one another. The coefficient has a value between -100% and +100% (-1 to +1). If the value is 0, the parameters are independent; if it is below or above zero, the parameters depend on each other partially; if the value is positive a simultaneous increase of both parameters will result in a similar fit; if the value is negative, then increasing one parameter and decreasing the other will lead to a similar fit; if the value is -1 or +1 the parameters completely depend on one another. Details about the calculation of confidence ellipses can be found in [2].

*High-temperature and high-pressure crystal chemistry*, Reviews in Mineralogy and Geochemistry, 41, 35-60. Copyright © 1997 - 2012 Mineralogical Society of America. All rights reserved

**F-f-plot**

The F-f plot is another visual quality assessment tool for finite strain EoS, where f_{E} (abscissa) is plotted against F_{E}(y-axis), a 'normalised' stress. Based on the F-f plot one can determine the compressional behavior of a material.

a) Data points plot on a horizontal line of constant F; K' = 4; data can be fitted with a 2^{nd} order BMEOS.

b) Data points plot on an inclined straight line; slope is equal to 3K_{0}(K'-4)/2; data can be fitted with a 3^{rd} order BMEOS.

c) Data points plot on a parabolic curve; K'' differs from implied value; f^{2} ≠ 0.

**Sources of error**

- Uncertainties in volume measurement (incl. V
_{0}errors) - Uncertainties in pressure determination
- Small data-set (low number of data points)

**Guest Lecturer**

"Equations of State" Prof. Ross J. Angel

Part 1 (35 minutes) ( 42.3MB Sep12 12)

Part 2 (60 minutes) ( 70.5MB Sep12 12)

**Literature**

[1] Anderson, O.L. (1995) *Equations of State of Solids for Geophysics and Ceramic Science*. Oxford University Press, Oxford, 405 pp.

[2] Angel, R.J. (2000) Equations of state. In: R.M. Hazen and R.T. Downs (Eds.) *High-temperature and high-pressure crystal chemistry*, Reviews in Mineralogy and Geochemistry, 41, 35-60.

[3] Duffy, T.S. and Wang, Y. (1998) Pressure-volume-temperature equations of state. In: R.J. Hemley (Ed.) *Ultrahigh-pressure mineralogy: physics and chemistry of the Earth's deep interior*, Reviews in Mineralogy, 37, 425-457.

[4] Poirier, J.P. (2000) *Introduction to the Physics of the Earth Interior.* Second edition, Cambridge University Press, Cambridge, 312 pp.

**Technical Papers:**

[5] Murnaghan, F.D. (1937) Finite deformations of an elastic solid. American Journal of Mathematics, 59, 235–260.

[6] Birch, F. (1947), Finite elastic strain of cubic crystals, Physical Review, 71, 809-824.

[7] Stacey, F. D., Brennan, B. J. and Irvine, R. D., 1981. Finite strain theories and comparisons with seismological data. Geophysical Surveys, 4, 189-232.

[8] Jeanloz, R. (1988) Universal Equation of State. Physical Review B, 38, 805-807.

**Problem Set**

EoS Homework (Acrobat (PDF) 1.9MB Jan19 12)

**Related Links**

For more information about Equations of State follow the links below:
- Chapter 5 of Don Anderson's book Theory of the Earth. Blackwell Scientific Publications (1989).
- Poirier, J.P. (2000)
*Introduction to the Physics of the Earth Interior.*Second edition, Cambridge University Press, Cambridge, 312 pp. - Chapter 4 talks about equations of state

**Acknowledgements**

These materials are being developed with the support of COMPRES, the Consortium for Materials Properties Research in Earth Sciences, under NSF Cooperative Agreement EAR 10-43050 and is partially supported by UNLV's High Pressure Science and Engineering Center, a DOE NNSA Center of Excellence supported under DOE NNSA Cooperative Agreement No. DE FC52-06NA26274.