As mentioned at the introduction, faulting folding and metamorphism are a consequence of the movement of the plates that form the earth’s crust. In areas of plate divergence, tension causes the ripping of the plates leading to the development of predominantly simple faults, termed normal or extensional, with the broken fragments simply falling due to gravity, and arranging themselves in an array of rifts, with the lower blocks forming “grabens”, and the upper ones “horsts”.
On the other side, on areas of plate convergence, extreme compression fields will cause the development of thrust faulting and intense folding. Both, the diverging as well as the converging zones encompass huge areas, developing topographical features with spectacular characteristics, particularly noticeable on aerial and/or satellite photography, but also as normal scenery.
- In rifting areas, the horsts tend to have an overall flat surface. A good example is the highest point of Portugal, Torre, at Serra da Estrela, with an elevation of approximately 2000m and, as figure 125 shows, it has a rather dull flat top.
- On the other hand, in converging boundaries the intense thrust faulting and tight folding give rise to a very rugged topography of sharp peaks surrounded by entrenched valleys, as for example the Alps (fig. 46).
Faulting takes place when the rocks under stress are brittle. Of the simple faults associated with Diverging Plate Boundaries, I only have the photo of a miniature graben (fig. 127) which, when it has its relevant dimensions is the main form of a rift valley.
Of the other simple faults, I only have two photos of rather small, but quite explanatory reverse examples. In figure 128, the proof that it is a reverse fault is that there is a duplication of the dyke within the dyke/fault vertical projection. In other words, the block on the right was pushed up. So, that is the upthrow side.
In figure 129 the dragging of the sediments on the upthrow side makes quite clear which way the movement went.
All the fault photos shown so far, are from artificial land cuttings that is, they show cross sections, which is the easiest way to visualise a fault. However, this is not the most common view of a fault when doing field work. In fact, with the large ones we only become aware of them when the geology is plotted on a map, where the fault appears as a linear structure offsetting the stratigraphic succession across which it cuts. Figure 129B is an exceptional example because it shows the fault and its displacement on a horizontal land surface and it is only observable because the fault is tiny. As it can be seen, the sedimentary beds dip towards the photographer and to the right of the fault the bedding plane strike lines are further away. Thus, the right hand side fault block is the downthrow side since it dropped relative to the other one and as the erosion leveled the ground, the strike lines were displaced towards a higher bedding plane position. As we used to say, the downthrow side moves up-dip.
Of the thrust faults, which tend to be quite flat, the only one I have is not so clear, but it gives the general idea (fig. 130).
Other items related to faulting are:
– Slickensided fault plane, defined as the polished and smoothly striated surface that results from the friction along a fault plane. Figure 131, is an example of a thrust fault, because the striations are almost horizontal. Also, the movement of the block nearest to the observer, was from right to left, since the sharper angle of the humps tend to be predominantly on the left side.
– Fault breccia, defined as the assemblage of angular fragments resulting from the crushing and shattering of rocks during the movement on the fault, is shown in figure 132.
– Mylonite is defined as a compact rock with a streaky or banded structure produced by the extreme granulation and shearing of the rocks pulverised during the thrusting. The development of very high pressure and temperature causes partial melting, giving the rock the appearance of a micro-brecciated toffee (fig. 133).
Finally, as mentioned above, faulting takes place under brittle environments. The stress release in such fields tend to develop fault sets that are close to perpendicular to each other and they are termed Conjugate Faults. Again, evidence of such occurrences are far more evident in a global scale and become very distinct when they are sufficiently strong to control the geomorphology . Once more I make use of Google maps to show a rather striking example, where the Douro River, in the North of Portugal, at one stage flows on an almost straight line in a SSW direction, to sharply veer to another very straight line, but now in a WNW direction (centre of figure 133B). Those lines are so straight that there can be no doubt that they represent a strong set of conjugate faults.
Folding takes place when the rocks are sufficiently plastic. That is, it occurs at considerable depths under compressional conditions, which means, Converging Plates environments. The simplest folds are the syncline, where the fold forms the bottom of a trough, and the anticline, where the fold forms the crest. Figure 134 shows a simple synclinorium with a broad anticline on the left, followed by a broad syncline on the right.
In figure 135 we have a small anticline, well delineated because of the thinly bedded sediments on which it occurs.
In the case of figure 136 the anticline is quite tilted, that is, overturned.
Both these anticlines are small scale examples of the gigantic folding common in orogenic regions. The first within the Cape Folded Belt in South Africa and the second within the Lower Alentejo Flysh Group in Portugal. Much more complete, but very seldom observable, is the grand view of a regional overturned synclinorium with a dimension of kilometers, also within the Cape Folded Belt (fig. 137).
Just to finalize folding, figures 138 and 139 show two examples of chevron folds, which are most aptly named.
7.4 Metamorphism / Metasomatism
Wikipedia defines metamorphism as the change of the minerals and structure of a preexisting rock by extreme heat and pressure, without causing its complete melting into a magma. This is the part of geology I like least and as such the one of which I know even less. Within the subduction zone, solid rocks may be remobilized to the extreme of becoming magma again. In the case of only partial remobilisation, when the initial rocks originate from a continental mass, they will have an acid composition and will be metamorphosed to gneisses. Figure 140 is an example of high level remobilization giving rise to a gneiss, where the white streaks are the remaining evidence of some thin quartz rich sedimentary beds which now give an appearance of flowing.
In the case of figure 141, if it was not for the presence of a resistant sedimentary remnant (xenolith), it would not be possible, by the naked eye, to determine if it was a granite or a gneiss.
Finally, the rock shown in figure 142, on first impression can very easily be considered a granite conglomerate, but in fact it is a greisen, defined by Wikipedia, as a light coloured rock containing quartz, mica and fluorine rich minerals. It results from the hydrothermal alteration of a granite, during the high gas and water rich cooling stages of emplacement. The fluids are forced into the interstitial spaces, thus giving the rock that conglomeritic appearance. Such a rock is quite common in the Castromil area of Portugal where I prospected for gold. Unfortunately the photographs from there were mislaid so I opted to use this one from Okiep in South Africa.
At Castomil I was told by a Chilean geologist that those rocks were definitely greisen and in Chile it was always associated with thrust faults in the vicinity of magmatic rocks. That is, identical to the Castromil circumstances.
Stylolites, Wikipedia defines, “as serrated surfaces at which mineral material has been removed by pressure dissolution, in a process that decreases the total volume of rock. Insoluble minerals remain within the stylolites making them visible”. This volume reduction may be caused by overburden or tectonic pressures. They are very common in limestones but are generally quite difficult to recognize, as for example the one shown in figure 111, just to the left of the pen. I do not think such a topic really belongs here, but I do not know where else I can put it and the one shown in figure 142B is the largest I have ever seen and it is very well highlighted by weathering. That is why I had to show it somewhere.