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STRUCTURAL ANALYSIS
Structural geology uses micro- and meso-scale structures found in the rocks to elaborate tools and
methods enabling to identify structures too large to be directly observed, although satellite imagery
now may help in this task. This lecture summarises standardised techniques used to unravel the shape,
extent, and arrangement of structures on a regional scale, together with the relative time sequence in
which the structures have appeared. Structural analyses designate investigations of geometric
features in the rocks to elucidate large-scale structures and tell their history.
Basic concepts
The study of primary and secondary structures is not a straightforward undertaking because outcrops
are often scarce or not available in critical areas, which makes direct observation of large structures
impossible and correlative interpretation, therefore, necessary. Furthermore, the geological
observation is essentially two dimensional because the relief is generally small compared to the map
area. Consequently, interpretation is still necessary to produce a three-dimensional picture, even in
areas of almost continuous outcrop.
Structural geologists must additionally reconstruct the deformation history of the rocks from the
patterns of primary and secondary structures found in the field. This aim implies fieldwork, i.e. direct
observation of rocks in their natural environment (outcrops, landscapes, drill cores). The belief is that
every feature is the record of an event that the scrutinized outcrop has experienced. It is assumed that
changes of structural orientations preserve changes in strain or stress axes. Thus, elucidating the
deformation history depends on the recognition of the relative age of different structures, such as
faults, folds and fabrics, using crosscutting or overprinting relationships.
In short, a successful structural analysis produces:
1) A geometric model, which is a three-dimensional picture that adequately describes the spatial
problems on the studied area.
2) A kinematic model, which is an account of the successive stages through which the studied
structure developed.
3) An indication of the directions and senses of the local movements that have affected the rocks.
4) A mechanical model, which attempts to determine the strain or stress history of the region.
We start by presenting basic concepts that are essential in deciphering the structural history of an
area. We then discuss the techniques traditionally employed in the interpretation of areas that have
suffered a single episode of deformation and areas that have been subjected to multiple deformations.
We will see that these concepts rely on often non-reciprocal propositions, which means that answers
are correct but not unique.
Analytic elements
Techniques appropriate to the study of simple areas, where structures have constant trends in rocks
with continuous bedding, formed the basis of structural analyses. They consider several types of
structural elements.
Scale
There are classically three scales of investigation: macroscopic, mesoscopic, and microscopic.
- Microscopic scale pertains to any structure so small (<10-2 m) that it requires to be examined with
an optical or electron microscope.
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Microscopic structures
From Bard 1990: Microtextures des roches magmatiques
et métamorphiques. Masson, Paris, 208p.
- Mesoscopic scale pertains to any structure that can be observed without the aid of the microscope
-2 2
on a hand specimen or a single outcrop (10 to 10 m).
- Macroscopic scale pertains to structures that are too large (>102 m) to be completely exposed in
one outcrop, which implies the interpretative step of reconstructing the structure from data collected
at a number of outcrops.
In understanding the structure of an area, the geologist is concerned principally with the mesoscopic
and macroscopic scales. Microscopic observations better establish the detailed characteristics of
features, such as foliations, that are visible on a mesoscopic scale. The concept of scale is very
important in structural geology. One must be constantly aware of the relationships between structures
at all scales, and intellectually jump from one scale observation to another to solve the geometrical
problems met in the field.
Stratigraphic sequence - Lithology
The establishment of the lithological and/or stratigraphic sequence is a prerequisite in interpreting the
large-scale structure and the history of an area. Any structural information has little meaning out of
its lithological (sedimentological or petrological) and age (paleontological or radiometric) context.
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- An interruption of stratigraphic contacts points to faults or unconformity that may not outcrop.
- Repetition of a stratigraphic sequence helps perceiving the positions of folds or thrusts.
The warning point concerns sequences of lithological units. For example, layering in deformed
metamorphic rocks does not necessarily represent bedding. Thus it is important, wherever possible,
to demonstrate the existence of bedding and stratigraphy, which can be obtained by identification of
sedimentary structures that define the “way up” of the beds. Selecting a distinctive marker horizon is
useful to picture regional structures.
Remember also triviality: a deformation structure is necessarily younger than hosting rocks and an
unconformity marks the time of a major tectonic event.
Mapping - Collection of Data
Geologic mapping is the foundation of any geological work because it is the only way to (1) make an
inventory of rock units and describe them; (2) recognise structures, document their complexity and
measure their orientations; (3) observe the nature of contacts between rock units and, in turn, disclose
the sequential history of major events; (4) make and check first hypotheses in the field and, finally
(5) construct cross sections to investigate the three-dimensional geometry of an area. These aspects
require iteration to develop a dynamic or kinematic history of the rock.
A field map represents as many measurements as possible and shows the distribution of the outcrops.
All data must be plotted at the site of observation on the map. They comprise:
- Stratigraphic data, including directions of younging, which is very important to discover the
geometrical configuration of a complexly deformed region.
- The trace and orientation of any structure. Penetrative structures are too thin to be drawn exactly
to scale and are generally treated as conventional symbols.
Modern geological mapping often combines satellite imagery or aerial photography with ground
operations.
The resulting geological map shows with colours and/or appropriate patterns the distribution of rock
formations at the earth’s surface. Accompanying structural maps display directional symbols that
enable identifying at a glance the dip direction of bedding and foliation planes and areas in which
they are folded. They also reveal the local vergence of small folds and the traces of axial plane
foliations.
Orientation data
Dips and strikes and other orientation data must be reported on geological maps. In complex,
‘polyphase’ areas systematic measurement is very important because late structures generally
disperse attitudes of earlier-structures, thus produce a wide variation in orientation data. In addition
to field measurements, fabric analysis can be obtained from the study of orientated samples. A
structural sample is actually always orientated.
The widespread belief is that orientation can assist in grouping structures of the same generation.
However, the fact that two structures have the same orientation does not necessarily mean that they
belong to the same group or family and conversely structures of a given group need not have the same
orientation (the variability in orientation structure). Always remember that the orientation of late fold
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axes may also depend on the orientation of earlier structures (e.g. inherited dip of a refolded plane
affects the orientation of fold axes).
Planar elements
The attitude of any planar element (bedding, foliations, etc...) is represented by its strike and by its
dip.
Remember:
- the strike is the compass direction of the horizontal line lying in an inclined plane;
- the dip is the large angle made by the plane with the horizontal and is measured
perpendicular to strike in the vertical plane.
For convenience, some geologists measure directly the dip-direction and the dip.
The international convention is to draw a T on the map with the top line parallel to the strike of the
plane and the leg indicating the dip direction of the bed. The azimuth is indicated by a three-figure
number recording the degrees clockwise beginning at north (thus ranging from 000 to 360), and the
dip by a two figure number that varies from 00 to 90, complemented with the approximate down-
dip direction (e.g. N). Azimuths must be expressed as 3-digit numbers (e.g. 045, not 45) to avoid
confusion of < 90 directions with dips.
The apparent width w of a layer on map is related to its thickness t and its dip θ by the simple
trigonometric equation:
t = w.sinθ
Linear elements
The attitude of a linear structure is described by its trend and its plunge.
Structural analysis jpb, 2017
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