Chapter 8 Measuring Geological Time
8.2 Relative Dating Methods
The simplest and most intuitive way of dating geological features is to look at the relationships between them. There are a few simple rules for doing this, some of which we’ve already looked at in Chapter 6. For example, the principle of superposition states that sedimentary layers are deposited in sequence, and, unless the entire sequence has been turned over by tectonic processes or disrupted by faulting, the layers at the bottom are older than those at the top. The states that any rock fragments that are included in rock must be older than the rock in which they are included. For example, a in an igneous rock or a clast in sedimentary rock must be older than the rock that includes it (Figure 8.2.1).
The states that any geological feature that cuts across, or disrupts another feature must be younger than the feature that is disrupted. An example of this is given in Figure 8.2.2, which shows three different sedimentary layers. The lower sandstone layer is disrupted by two , so we can conclude that the faults are younger than that layer. But the faults do not appear to continue into the coal seam, and they certainly do not continue into the upper sandstone. So we can infer that coal seam is younger than the faults (because it cuts them off), and of course the upper sandstone is youngest of all, because it lies on top of the coal seam.
The outcrop shown here (at Horseshoe Bay, B.C.) has three main rock types:
- Buff/pink felsic intrusive igneous rock present as somewhat irregular masses trending from lower right to upper left
- Dark grey metamorphosed basalt
- A 50 centimetres wide light-grey felsic intrusive igneous dyke extending from the lower left to the middle right – offset in several places
Using the principle of cross-cutting relationships outlined above, determine the relative ages of these three rock types.
(The near-vertical stripes are blasting drill holes. The image is about 7 metres across.)
See Appendix 3 for Exercise 8.1 answers.
An represents an interruption in the process of deposition of sedimentary rocks. Recognizing unconformities is important for understanding time relationships in sedimentary sequences. An example of an unconformity is shown in Figure 8.2.4. The Proterozoic rocks of the Grand Canyon Group have been tilted and then eroded to a flat surface prior to deposition of the younger Paleozoic rocks. The difference in time between the youngest of the Proterozoic rocks and the oldest of the Paleozoic rocks is close to 300 million years. Tilting and erosion of the older rocks took place during this time, and if there was any deposition going on in this area, the evidence of it is now gone.
There are four types of unconformities, as summarized in Table 8.1, and illustrated in Figure 8.2.5.
|Nonconformity||A boundary between non-sedimentary rocks (below) and sedimentary rocks (above)|
|Angular unconformity||A boundary between two sequences of sedimentary rocks where the underlying ones have been tilted (or folded) and eroded prior to the deposition of the younger ones (as in Figure 8.2.4)|
|Disconformity||A boundary between two sequences of sedimentary rocks where the underlying ones have been eroded (but not tilted) prior to the deposition of the younger ones (as in Figure 8.2.2)|
|Paraconformity||A time gap in a sequence of sedimentary rocks that does not show up as an angular unconformity or a disconformity|
- Figures 8.2.1ab, 8.2.2, 8.2.3, 8.2.4, 8.2.5: © Steven Earle. CC BY.
the principle that inclusions within a body of rock must be older than the rock
a fragment of country incorporated into igneous rock, commonly as a result of stoping
the principle that a body of rock that cuts across or through another body of rock is younger than that other body
a boundary in rock or sediment along which displacement has taken place
a geological boundary at the base of a sedimentary layer