Fracture (geology)

Cracks in rock are a mechanism of brittle deformation in response to stress

A fracture is any separation in a geologic formation, such as a joint or a fault that divides the rock into two or more pieces. A fracture will sometimes form a deep fissure or crevice in the rock. Fractures are commonly caused by stress exceeding the rock strength, causing the rock to lose cohesion along its weakest plane.^[1] Fractures can provide permeability for fluid movement, such as water or hydrocarbons. Highly fractured rocks can make good aquifers or hydrocarbon reservoirs, since they may possess both significant permeability and fracture porosity.

Brittle deformation

Fractures are forms of brittle deformation.^[2] There are two types of primary brittle deformation processes. Tensile fracturing results in joints. Shear fractures are the first initial breaks resulting from shear forces exceeding the cohesive strength in that plane.

After those two initial deformations, several other types of secondary brittle deformation can be observed, such as frictional sliding or cataclastic flow on reactivated joints or faults.

Most often, fracture profiles will look like either a blade, ellipsoid, or circle.

Causes

The concentric circles in this sandstone are "plumose" (plume-like) structures that can form during the formation and propagation of a fracture

Fractures in rocks can be formed either due to compression or tension. Fractures due to compression include thrust faults. Fractures may also be a result from shear or tensile stress. Some of the primary mechanisms are discussed below.

Modes

First, there are three modes of fractures that occur (regardless of mechanism):

Mode I crack – Opening mode (a tensile stress normal to the plane of the crack)
Mode II crack – Sliding mode (a shear stress acting parallel to the plane of the crack and perpendicular to the crack front)
Mode III crack – Tearing mode (a shear stress acting parallel to the plane of the crack and parallel to the crack front)

For more information on this, see fracture mechanics.

Tensile fractures

This deformation creates propagation of fractures into previously unfractured rock, when the rock is subjected to tensile stress. In the case of a homogenous stress field, the crack will propagate in the direction perpendicular to the least principal stress.

Engineers studying elasticity found that the stress due to a load distant from the region of interest is concentrated around material flaws. A. W. Griffith took this example and applied the concept of stress concentration to the ends of fractures. Griffith asserted that all material have microcracks or flaws where the stress concentration naturally occurs, and that these were the flaws where, under increasing stress, fractures propagate.^[3] As a result, these pre-existing flaws were named Griffith cracks, and allow the conceptual assumption that rocks are relatively weak.

From this assumption, tensile fracture development may be examined.

The first form is in axial stretching'. In this case, remote tensile stress is applied, allowing microcracks to open slightly throughout the tensile region. As these cracks open up, the stresses at the crack tips intensify, eventually exceeding the rock strength and allowing the fracture to propagate. This can occur at times of rapid overburden erosion. Folding also can provide tension, such as along the top of an anticlinal fold axis, where the tensile forces associated with the stretching of the upper half of the layers during folding can induce tensile fractures parallel to the fold axis.

Tensile fracturing may also be induced by applied compressive loads along an axis, which results in longitudinal splitting. In this situation, tiny tensile fractures form parallel to the loading axis, however the load forces any other microfractures closed. To picture this, imagine an envelope, with loading from the top. A load is applied on the top edge, the sides of the envelope open outward, even though nothing was pulling on them. Rapid deposition and compaction can sometimes induce these fractures.

For Griffith Fractures, there are several key equations.

K_I = Δσ(πa)^½

when

K_IC = K_I

the fracture is propagated, where K_I is the stress concentration at the fracture tip, Δσ is the difference in stress applied along the fracture area and the in-situ stress, and a is the half length of the fracture.

W(x) = 4∙((1 − ν²)/E)∙Δσ∙(a² − x²)^½

where W(x) is the fracture width at x distance from the center, ν is the Poisson's ratio, E is the Young's Modulus of Elasticity, Δσ is the difference in stress applied along the fracture area and the in-situ stress, and a is the half length of the fracture.

Another tensile fracture mechanism is hydraulic fracturing. In a natural environment, this occurs when a combination of rapid sediment compaction and thermal fluid expansion causes the pore fluid pressure to exceed the pressure of the least principal normal stress. When this occurs, a tensile fracture opens perpendicular to the plane of least stress.^[4]

Tensile fractures are almost always referred to as joints, which are fractures where no appreciable slip or shear is observed.

Joint types^[3]

Describing joints can be difficult, especially without visuals. The following are descriptions of typical natural fracture joint geometries that might be encountered in field studies:

Plumose Structures are fracture networks that form at a range of scales, and spread outward from a joint origin. The joint origin represents a point at which the fracture begins. The mirror zone is the joint morphology closest to the origin that results in very smooth surfaces. Mist zones exist on the fringe of mirror zones and represent the zone where the joint surface slightly roughens. Hackle zones predominate after mist zones, where the joint surface begins to get fairly rough. This hackle zone severity designates barbs, which are the curves away from the plume axis.
Orthogonal Joints occur when the joints within the system occur at mutually perpendicular angles to each other.
Conjugate Joints occur when the joints intersect each other at angles significantly less than ninety degrees.
Systematic Joints are joint systems in which all the joints are parallel or subparallel, and maintain roughly the same spacing from each other.
Columnar Joints are joints that cut the formation vertically in (typically) hexagonal columns. These tend to be a result of cooling and contraction in hypabyssal intrusions or lava flows.
Desiccation cracks are joints that form in a layer of mud when it dries and shrinks. Like columnar joints, these tend to be hexagonal in shape.
Sigmoidal Joints are joints that run parallel to each other, but are cut by sigmoidal (stretched S) joints in between.
Sheeting joints are joints that often form near surface, and as a result form parallel to the surface. These can also be recognized in exfoliation joints.
In joint systems where relatively long joints cut across the outcrop, the throughgoing joints act as master joints and the short joints that occur in between are cross joints.
Poisson effect is the creation of vertical contraction fractures that are a result of the relief of overburden over a formation.
Pinnate joints are joints that form immediately adjacent to and parallel to the shear face of a fault. These joints tend to merge with the faults at an angle between 35 and 45 degrees to the fault surface.
Release joints are tensile joints that form as a change in geologic shape results in the manifestation of local or regional tension that can create Mode I tensile fractures.
Concurrent joints that display a ladder pattern are interior regions with one set of joints that are fairly long, and the conjugate set of joints for the pattern remain relatively short, and terminate at the long joint.
Sometimes joints can also display grid patterns, which are fracture sets that have mutually crosscutting fractures.
An en echelon or stepped array represents a set of tensile fractures that form within a fault zone parallel to each other.

Faults and shear fractures

Faults are another form of fracture in a geologic environment. In any type of faulting, the active fracture experiences shear failure, as the faces of the fracture slip relative to each other. As a result, these fractures seem like large scale representations of Mode II and III fractures, however that is not necessarily the case. On such a large scale, once the shear failure occurs, the fracture begins to curve its propagation towards the same direction as the tensile fractures. In other words, the fault typically attempts to orient itself perpendicular to the plane of least principal stress. This results in an out-of-plane shear relative to the initial reference plane. Therefore, these cannot necessarily be qualified as Mode II or III fractures.^[3]

An additional, important characteristic of shear-mode fractures is the process by which they spawn wing cracks, which are tensile cracks that form at the propagation tip of the shear fractures. As the faces slide in opposite directions, tension is created at the tip, and a mode I fracture is created in the direction of the σ_h-max, which is the direction of maximum principal stress.

Shear-failure criteria is an expression that attempts to describe the stress at which a shear rupture creates a crack and separation. This criterion is based largely off of the work of Charles Coulomb, who suggested that as long as all stresses are compressive, as is the case in shear fracture, the shear stress is related to the normal stress by:

σ_s= C+μ(σ_n-σ_f),^[3]

where C is the cohesion of the rock,or the shear stress necessary to cause failure given the normal stress across that plane equals 0. μ is the coefficient of internal friction, which serves as a constant of proportionality within geology. σ_n is the normal stress across the fracture at the instant of failure, σ_f represents the pore fluid pressure. It is important to point out that pore fluid pressure has a significant impact on shear stress, especially where pore fluid pressure approaches lithostatic pressure, which is the normal pressure induced by the weight of the overlying rock.

This relationship serves to provide the coulomb failure envelope within the Mohr-Coulomb Theory.

Frictional sliding is one aspect for consideration during shear fracturing and faulting. The shear force parallel to the plane must overcome the frictional force to move the faces of the fracture across each other. In fracturing, frictional sliding typically only has significant effects on the reactivation on existing shear fractures. For more information on frictional forces, see friction.

One important idea when evaluating the friction behavior within a fracture is the impact of asperities, which are the irregularities that stick out from the rough surfaces of fractures. Since both faces have bumps and pieces that stick out, not all of the fracture face is actually touching the other face. The cumulative impact of asperities is a reduction of the real area of contact', which is important when establishing frictional forces.^[3]

Subcritical crack growth

Sometimes, it is possible for fluids within the fracture to cause fracture propagation with a much lower pressure than initially required. The reaction between certain fluids and the minerals the rock is composed of can lower the stress required for fracture below the stress required throughout the rest of the rock. For instance, water and quartz can react to form a substitution of OH molecules for the O molecules in the quartz mineral lattice near the fracture tip. Since the OH bond is much lower than that with O, it effectively reduces the necessary tensile stress required to extend the fracture.^[3]

Engineering considerations

In geotechnical engineering a fracture forms a discontinuity that may have a large influence on the mechanical behavior (strength, deformation, etc.) of soil and rock masses in, for example, tunnel, foundation, or slope construction.

Fractures also play a significant role in minerals exploitation. One aspect of the upstream energy sector is the production from naturally fractured reservoirs. There are a good number of naturally fractured reservoirs in the United States, and over the past century, they have provided a substantial boost to the nation's net hydrocarbon production.

The key concept is while low porosity, brittle rocks may have very little natural storage or flow capability, the rock is subjected to stresses that generate fractures, and these fractures can actually store a very large volume of hydrocarbons, capable of being recovered at very high rates. One of the most famous examples of a prolific naturally fractured reservoir was the Austin Chalk formation in South Texas. The chalk had very little porosity, and even less permeability. However, tectonic stresses over time created one of the most extensive fractured reservoirs in the world. By predicting the location and connectivity of fracture networks, geologists were able to plan horizontal wellbores to intersect as many fracture networks as possible. Many people credit this field for the birth of true horizontal drilling in a developmental context. Another example in South Texas is the Georgetown and Buda limestone formations.

Furthermore, the recent uprise in prevalence of unconventional reservoirs is actually, in part, a product of natural fractures. In this case, these microfractures are analogous to Griffith Cracks, however they can often be sufficient to supply the necessary productivity, especially after completions, to make what used to be marginally economic zones commercially productive with repeatable success.

However, while natural fractures can often be beneficial, they can also act as potential hazards while drilling wells. Natural fractures can have very high permeability, and as a result, any differences in hydrostatic balance down the well can result in well control issues. If a higher pressured natural fracture system is encountered, the rapid rate at which formation fluid can flow into the wellbore can cause the situation to rapidly escalate into a blowout, either at surface or in a higher subsurface formation. Conversely, if a lower pressured fracture network is encountered, fluid from the wellbore can flow very rapidly into the fractures, causing a loss of hydrostatic pressure and creating the potential for a blowout from a formation further up the hole.

Fracture terminology

A list of fracture related terms:^[3]

fracture – any surface of discontinuity within a layer of rock
vein – a fracture filled with minerals precipitated out of an aqueous solution
dike – a fracture filled with sedimentary or igneous rock not originating in the fracture formation
joint – a natural fracture in the formation in which there is no measureable shear displacement
shear fracture – fractures across which shear displacement has occurred
fault – (in a geologic sense) a fracture surface upon which there has been sliding
fracture trace – the line representing the intersection of the fracture plane with the surface
fracture tip – the point at which the fracture trace terminates on the surface
fracture front – the line separating the rock that has been fractured from the rock that has not
Griffith cracks – preexisting microfractures and flaws in the rock
axial stretching – fracture mechanism resulting from a remote applied tensile force that creates fractures perpendicular to the tensile load axis
longitudinal splitting – fracture mechanism resulting from compression along an axis that creates fractures parallel to the load axis
wing cracks – tensile fractures created as a result of propagating shear fractures
K_IC – critical stress intensity factor, aka fracture toughness – the stress intensity at which tensile fracture propagation may occur
asperities – tiny bumps and protrusions along the faces of fractures
pore fluid pressure – the pressure exerted by the fluid within the rock pores
lithostatic pressure – the weight of the overlying column of rock
cataclastic flow – microscopic ductile flow resulting from small grain-scale fracturing and frictional sliding distributed across a large area.

References

↑ Park, R. G. (2005) Foundation of Structural Geology (reprint of the 1997 Chapman and Hall edition) Routledge, Abingdon, England,page 9, ISBN 978-0-7487-5802-9
↑ https://www.researchgate.net/publication/256292479_Structural-temporal_approach_to_modeling_of_fracture_dynamics_in_brittle_media, Y.V. Petrov, St.-Petersburg State University & Inst Probl Mech Engng of the RAS, St.-Petersburg, Russia, 2013
1 2 3 4 5 6 7 Van Der Pluijm, Ben A. and Marshak, Stephen (2004) Earth Structure- Second Edition W.W. Norton & Company, Inc. New York, New York, ISBN 0-393-92467-X
↑ Secor, D. T., 1965. "Role of fluid pressure in jointing" American Journal of Science, 263, 633-646

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