Structural Geology

Structural Geology

Haakon Fossen

Language: English

Pages: 524

ISBN: 1107057647

Format: PDF / Kindle (mobi) / ePub


This market-leading textbook has been fully updated in response to extensive user feedback. It includes a new chapter on joints and veins, additional examples from around the world, stunning new field photos, and extended online resources with new animations and exercises. The book's practical emphasis, hugely popular in the first edition, features applications in the upper crust, including petroleum and groundwater geology, highlighting the importance of structural geology in exploration and exploitation of petroleum and water resources. Carefully designed full-colour illustrations work closely with the text to support student learning, and are supplemented with high-quality photos from around the world. Examples and parallels drawn from practical everyday situations engage students, and end-of chapter review questions help them to check their understanding. Updated e-learning modules are available online (www.cambridge.org/fossen2e) and further reinforce key topics using summaries, innovative animations to bring concepts to life, and additional examples and figures.

 

 

 

 

 

 

 

 

 

 

 

 

 

of a propagating fault tip are called fault propagation folds. Thus, many drag folds are faulted fault propagation folds. However, drag can also form or become accentuated in the walls of an already existing fault. Just like the damage zone, fault drag can develop due to locking of the fault at fault bends, fault linkage and other complications that can increase the friction along faults. The effect of non-planar fault geometry is discussed in Chapter 20, and the development of normal drag

and even homogeneous in some cases. In this sense the concept of strain can also be applied to brittle deformation (brittle strain). The success of doing so depends on the scale of observation. zone, to look at some fundamental deformation types. We will think in terms of particle positions (or vectors) and see how particles change positions during deformation. If (x, y) is the original position of a particle, then the new position will be denoted (x 0 , y 0 ). For homogeneous deformation in two

performed during the deformation history. It does however not take into consideration the rotation of the strain ellipse that occurs for non-coaxial deformations (see Section 2.12) and is therefore best suited for coaxial deformations. An alternative strain diagram can be defined by means of "goct , where the natural octahedral unit shear is plotted against a parameter n called the Lode parameter, where n¼ 1 1 3 2 4 ln(Y/Z ) n 0.0 (b) −0.5 −1.0 3 Cigars 1.0 A pure volume change or

and normal stresses on the surface. When sn is oriented perpendicular to the fracture there is no shear stress on the surface, and the fracture is stable. In the general case there is a (resolved) shear stress on the fracture, and the friction constrains the reactivation potential. That local friction on the fracture is commonly referred to as the coefficient of sliding friction (mf ). The coefficient of sliding friction is simply the shear stress required to activate slip on the fracture divided

displacement in the central part of the fault trace, gradually decreasing toward the tips, as illustrated in Figure 8.13. The shape of the displacement profile may vary from linear to bell-shaped or elliptic. Displacement profiles are sometimes classified into those that have a well-defined central maximum (peak type) and those that have a wide, central part of fairly constant displacement (plateau type). Examples are shown in Figure 8.14. L Figure 8.14 Types of displacement (D) profiles along

Download sample

Download