Stress, Strain and Their RelationshipMarianne Casamatis, Laura Matarese, Danielle Sharpe and Katherine
Zunica


Table of
contents PART 1 1) Introduction PART 2  STRESS 2) What is stress?  force and traction 3) Stress acting on a plane  Mohr diagram 4) Stress acting on a point  the stress ellipsoid  properties of the stress ellipsoid  principal stress axes  the stress tensor PART 3  STRAIN 5) What is strain? 6) Types of Strain : Homogeneous vs. Heterogeneous 7) The Strain Ellipsoid 8) The Flinn Diagram 9) The Finite Strain Ellipsoid 10) Strain Path  Coaxial  Non coaxial 11) Incremental and Finite Strain  The incremental strain ellipsoid 12) Strain regime : pure shear vs. simple shear PART 4  THE STRESS/STRAIN RELATIONSHIP 13) Indications of stress and strain. 14) Smallscale strain features in the tectonic regime. 15) Pure and Simple Shear in nature 16) Incremental strain and Kinematics analysis 17) Stress Perturbation PART 5  Conclusion, References and Glossary 

IntroductionThis report gives an overview of two important concepts within structural
geology; stress and strain. These concepts are important because they allow
us, to some extent, formulate and describe the deformation history
on both a micro and macro scale. The report will firstly outline how stress and strain are defined and then how the two concepts are related to one another. Stress can be defined in terms of force and traction. Stress can
be divided into two categories; stress on a plane and stress at a point.
Stress acting on a plane consists of two components; normal and shear stress.
Stress acting on a plane can be represented and calculated using the Mohr
diagram for stress (also outlined in the first section of the report).
Stress on a point can be visualised using the stress ellipsoid. The construction
and components of the stress ellipsoid, including the principal stress axes,
will be outlined in the first section of the report. Stress at a point can
also be defined mathemetically, using the stress tensor The second section of the report will deal with strain. It will outline what strain is and how it can be represented visually in terms of the strain ellipsoid. There will be a discussion of the two types of strain; homogeneous and heterogeneous. The Flinn diagram is important to the representation of strain. The Flinn diagram is a graph which shows all possible configurations of the strain ellipsoid in terms of the ratio of its axes, strain intensity and shape of the strain ellipsoid. We will discuss the strain path, which describes the intermediate stages during the process of straining, and this will include coaxial and non coaxial strain paths. We will then discuss incremental strain, and how it leads us to the Finite Strain Ellipsoid, then we will relate this to pure and simple shear. The final section of the report will discuss the nature of the relationship
between stress and strain. It will also look at ways of how we can derive
the orientation of the stress and finite strain ellipsoids from field observations. 

STRESS


Caption for figure below... 
Caption for figure above 

So, what is stress?
Stress can be calculated mathematically using this equation: Force/Area.
So, we can think of stress in terms of the intensity of force for a given area or a measure of how concentrated the force is.
Stress is usually measured in megapascals. (MPa). (1 N/m^2=1Pa)
Stress can be thought of as acting
on a surface or a point. Stress on a surface and a point will now be discussed.
Stress acting on a PlaneIn this section, we are examining stress acting on a single plane, and thus we are looking at stress in 2dimensions. As previously mentioned, stress is a vector. Stress can be acting in any orientation to a plane. Stress acting on a single plane can be reduced to two vector components (Pluijm etal, 1997). These are the normal stress component and the shear stress component. On either side of the plane, these components have opposing tractions
The normal stress component has the symbol sigma n. It is the stress component perpendicular to the plane. The shear stress component
has the symbol Tau or sigma s. It is the stress component that is parallel
to the axes of the plane. This will be shown in more detail, later in the
report. The Mohr Diagram for StressThe Mohr circle is a useful tool in structural geology. It is a graphical way to represent and calculate stress acting on a plane. The normal and shear stress components are calculated using the fundamental stress equations below. The diameter of the mohr circle is the differential stress (sigma 1  sigma 3). The vertical axis of the graph shows the magnitude of the shear stress component and the horizontal axis shows the magnitude of the normal stress component. Sigma 1 and sigma 3 lie on the horizontal axis as they are orthoganol to the plane and therefore contain no amount of shear stress.The diameter of the circle is indicative of the material's strength. The larger the diameter of the circle, the larger the strength of the material under stress. Theta in the diagram is the angle between the normal stress vector and the orientation of sigma 1.
Stress at a Point
a) The stress ellipsoidA point defines the intersection of an infinite number of planes, each with a different orientation (Pluijm etal, 1997). So, the state of stress acting on a point describes all the stresses acting on these planes. Each of these planes will have the normal and shear stress components that have been described above. The magnitudes of these components vary as a function of the orientation of the plane. This property can be illustrated in three dimensions to obtain the stress ellipsoid. Visually, the length
of the line of the stress vector is representative of the magnitude of the
stress applied. The length of the stress vector will vary due to the orientation
of the plane. Imagine this property being applied to the infinite number of
planes that a point intersects. This report will not comment on how the lengths
of the stress vectors are determined, only on what outcome we can derive
from them.
If we envelope these stress vectors, we obtain an ellipsoid. This is the stress ellipsoid. It fully describes the state of stress at a point (Pluijm etal, 1997).
The ellipsoid allows us to find the stress for any plane. b) Properties of the Stress EllipsoidAn ellipsoid is defined by three axes.
In the stress ellipsoid, these axes are defined as the principal stresses. These three principal stress axes are orthogonal to one another. They are also perpendicular to three plane These planes have the only orientation where the shear stresses are equal to zero. Thus the planes only have the normal stress acting on them (lec7 net reference). These three planes are called the principal planes of stress. However, in this report we are mainly concerned with the axes of the ellipsoid. The principal stresses are vectors. That is, they have magnitude and direction. We can describe the state of stress of a body by specifying the orientation and magnitude of these axes.
c) The Principal Stress axes The principal stress
axes of the stress ellipsoid are labelled sigma1, sigma2 and sigma3
1 is the principal stress axis (the direction of maximum stress) 2 is the intermediate principal stress axis. 3 is the least principal stress axis (the direction of minimum stress) Or, in mathematical terms, sigma1>sigma2>sigma3.
There are several common states of stress that can be defined by the relationships of the principal stresses. These stress states are isotropic, anisotropic and deviatoric. Types of anisotropic states of stress are uniaxial, biaxial and triaxial.
An isotropic state of stress is where all three principal stresses are equal in magnitude. The ellipsoid is actually a sphere in this case. sigma1=sigma2=sigma3
Anisotropic is a stress state where at least one axis has a different magnitude to the other axes. This describes an ellipsoid
Deviatoric stress is the part of the total stress that is left after the mean stress is removed. Deviatoric stress is equivalent to tectonic stress and is the sress responsible for deformation. Mean stress, sigma m, is given by sigma m=(sigma1+sigma2+sigma3)/3. Deviatoric stress has the symbol sigma dev. So, sigma total=sigma m + sigma dev
Uniaxial stress can be in tension or compression. The sign convention for tension in geology is negative, and compression is positive (Pluijm etal, 1997). The ellipsoid is 'needlelike'. Uniaxial tension: sigma1=sigma2=0; sigma3<0 (Pluijm etal, 1997). Uniaxial compression:
sigma2= sigma3= 0; sigma1>0.
Biaxial stress is where one axis equals zero. For example, sigma 1>0>sigma 3 The general triaxial state of stress is where none of the three principle stress axis can be zero. That is, sigma
1>sigma 2>sigma 3 The Stress TensorThe Stress Ellipsoid is one description for the state of stress at a point. There is also a mathematical description that defines this state of stress, called the Stress Tensor. We will briefly detail this mode of defining stress. For a more detailed explanation refer to the reference list. The orientation and magnitude of the state of stress of a body can be defined in terms of its components in a specific Cartesian reference frame. A Cartesian reference frame has three mutually perpendicular coordinate axes, X, Y, and Z. Or in this image X1, X2 and X3.
The image shows a stress acting on a plane (X1, X2). Its vector components are also shown on this image. The normal stress component is parallel to X3. The shear stress components are expressed as being parallel to X1 and X2. In three dimensions, we can think of the point of stress as a cube.
The stress acting
on the three faces perpendicular to the axes of the cube can be resolved
into their component parts. For example, the face normal to the X1 axis can
be resolved into its normal component, sigma11 and the shear components are
sigma12 and sigma13. This can be done for the face with the normal component
sigma22 and sigma33. This gives us a total of nine stress components. This
is given in the form of a matrix:
We can relate the
stress tensor cube to the stress ellipsoid. For example, the stress ellipsoid
has three principal planes of stress, where they contain no shear stress components.
We can consider this state on the cube.
The plane (X1, X2) can be oriented so there are no shear stress components and the normal components, 1, 2, 3 are left acting on these planes. These normal components represent the principal stresses. The matrix would be reduced to:

Strain is the response of rocks to stress. It describes the final shape of a rock in terms of the initial shape.
During deformation, a rock will change in size and shape. Deformation describes the complete transformation from the initial to the final geometry of a body, and can be broken down into 4 main components:
Translation (movement from one place to another)
Rotation (spin around an axis)
Distortion (change in shape)
Dilation (volume change)
Strain specifically relates to the changes of points in a body relative to each other.
From this we can see that strain relates to the distortion component of deformation.
There are two types of strain: Homogeneous and Heterogeneous.
The way we differentiate between the two is by examining marker lines drawn on an object both before and after deformation.
Straight marker lines remain straight after homogeneous deformation.
Straight marker lines become curved after heterogenous deformation.
Homogeneous strain results when any two portions of a body which were similar
in form and orientation before strain, are still similar in form and orientation
after the strain.
As a consequence, straight lines remain straight, parallel lines remain parallel, and planar surfaces remain planar.
In two dimensions, circles will become ellipses, and in three dimensions spheres will become ellipsoids
Caption... 

Strain is heterogeneous when it varies across the surface of an object.
Changes in the size and shape of small parts of the body are proportionately different from place to place.
As a consequence, straight lines become curved, planes become curved surfaces, and parallel lines generally do not remain parallel after deformation.
This implies the presence of a strain gradient.
This is represented in the diagram below. ****

Captions...... 
In order to analyse a heterogeneously strained body, we need to break it down into homogeneous portions. We therefore divide a deformed body into volumes that are small enough for the deformation to be described as locally homogeneous.

Captions.... 
This can be seen in figure ******** above. The picture on the left represents
the undeformed state. The picture on the right depicts heterogeneous strain
on the scale of the whole block. We divide the whole block into small sections,
as depicted by the yellow circles. At the scale of each individual cell containing
a yellow circle, the circles have been transformed into ellipses, and the
strain at each cell level is now homogeneous.
The strain ellipsoid is used as a three dimensional way to represent strain.
The strain ellipsoid results from the homogeneous deformation of an imaginary sphere, which represents the undeformed state of a body.
In any homogeneously strained, three dimensional body, there will be at least three lines of particles, also known as material lines, that will not rotate relative to each other. After strain, we will therefore have three material lines that remain perpendicular. These lines define the axes of an ellipsoid, and are known as the principal strain axes. They are referred to as X, Y and Z, where
X > Y > Z
X = maximum direction of extension
Y = intermediate strain axis
Z = maximum direction of shortening
These axes are also known
as lamda 1,2 and 3, where
_{
lamda 1 > lamda 2 > lamda
3}
The axes of the strain ellipsoid will therefore be different in length to the length of the axes in an undeformed sphere. This difference is a measure of the strain magnitude.

The finite strain ellipsoid (FSE) represents the end product of the homogeneous deformation of an imaginary sphere.
It does not give us any information about the strain history, or the mode of shear, that is, whether the shear was pure or simple.
For this we need to know about the strain path.
A rock does not undergo ductile deformation instantaneously. The strain
states that a rock will progressively pass through, to reach its final deformed
state, is known as the strain path.
In nature, we generally see rocks in their final strained state, and we
must deduce the initial undeformed state. The strain path gives us a description
of the intermediate stages during the process of straining.
Strain paths can be either coaxial or noncoaxial.
A coaxial strain path is where the strain axes are parallel to the same material lines throughout the straining.
Therefore, the principal axes of the strain ellipsoid do not rotate during deformation.
An example of this is pure shear.
A noncoaxial strain path is where the strain axes are parallel to different material lines during each infinitesimal increment of straining.
Therefore, the principal axes of the strain ellipsoid move through the material during deformation. At any given increment of strain, the principal axes lie in a different physical part of the deforming material.
An example of this is simple shear.
Most of the structures we see in nature reflect the total strain. The total strain is also referred to as the finite strain. It is independent of the intermediate steps. Finite strain can be the same for two rocks having different strain paths.
Incremental strain is the increment of distortion whose sum led to finite strain.
The finite strain is the sum of all of the incremental strains.
Incremental strain is represented by the Incremental Strain Ellipsoid (ISE).
The axes of the ISE do not change in orientation or magnitude from one increment to the next.
Figure ****** below represents the increments of strain during pure shear.
The incremental strain ellipse is at the bottom and does not change.

As already seen the FSE does not give us any information regarding the strain history.
The FSE can develop according to the two end members of strain regime: pure shear and simple shear
During pure shear, the principal axes of the FSE do not rotate during deformation.
During simple shear, the
magnitude and orientation of the axes of the FSE will change. The axes
of the FSE will rotate during deformation, and will not remain parallel to
the axes of the ISE. The rotation of the axes will give us information relating
to the kinematic of the deformation.
Often in nature both strain
regimes are present with one being dominant over the other and therefore dominating
the appearance of foliation, shear zones and features such as clasts and
rigid objects. Together they are called general shear, with symmetric
patterns indicating dominant pure shear and asymmetric patterns indicating
dominant simple shear.


Figure whatever..... 



Smallscale strain features in a tectonic regime.
Paleostress analysis uses the relationship between stress and strain to
examine the deformation history. This for example is a block in compression.
From the strain features present, the vertical styolitic joints, horizontal
extensional fractures and the en echèlon features some idea of the
stress acting upon the unit can be deduced. En echèlon features can
be an indication of incremental strain as new ones open up as a result of
strain over time.
Pure and Simple shear in nature.
As stated previously, general shear is more commonly found with either pure
or simple shear being the dominant regime.
The pictures below show,
on the left, a dominant simple shear regime, and on the right, a dominant
pure shear. Note the asymmetry of the left and symmetry on the right.


Incremental strain and Kinematics
analysis.
The ISE and the Incremental Strain Analysis (ISA) that can be done from
this are inextricably linked to the strain regime, as incremental strain
is the change of strain through time.
ISA is basically the relationship between the stress axis and strain axis,
and both axes have to be parallel to make a comparison. Pure shear, which
doesn’t rotate with time, can be analyzed. Simple shear cannot be analysed,
as while the stress axis remains constant with time, the strain axis rotates.
This rotation gives the kinematics of the deformation also known as internal
vorticity which is measured by its degree of non coaxiality or the degree
it has deviated from the original parallel relationship between δ1// λ3, δ3//λ1 and δ2// λ2.
Therefore Internal vorticity = Wk (kinematics vorticity number) and α = degree of deviation.
Then: Wk = Cos. α
When: Wk =0 pure shear.
0>Wk>1 general shear.
Wk =1 simple shear.
Stress
perturbation is a term used to describe the behavior of a stress field once
it looses its homogeneity.

logically if enough stress is placed on an area strain and distortion follows causing extensional fractures (an array of these is called en echèlon) with dominant simple shear. If the stress/strain force overwhelms the mechanical strength of an area a mechanical discontinuity/instability will occur, commonly called faults. *** this illustration shows one such scenario where an extensional fracture with dominant simple shear has been dissected and driven apart by a transform fracture/fault. This has the effect of mechanically isolating the total into two homogenous(isotropic) sections either side of the failure. These two sections are continuing to rotate under the stresses δ1 and δ3, that deformed the extensional fracture. But since they are now separate the bottom right section will continue in a clockwise direction and the upper left in an anticlockwise.
Conclusion 
References 
Glossary Material Lines : Lines that contain recognisable features, (for example, grains or fossils), that do not rotate relative to one another during deformation. 