Describing sedimentary rocks

An introduction to describing sedimentary rocks

 

                          

 

This page contains links to brief articles on the basics of describing sedimentary rocks, including grain size and grain size distribution, sandstone classification, and mineralogy.

Check out the companion How to… pages:

Common structural geology and mapping problems

Stratigraphy and sedimentology

Describing sedimentary rocks

Describing sedimentary rocks – some basics

Beds and bedding planes

Grain size of clastic rocks and sediments

Analysis of sediment grain size

Some controls on grain size distributions

 

Invertebrate morphology for sedimentologists

Bivalve morphology for sedimentologists

Trilobite morphology for sedimentologists

Gastropod shell morphology for sedimentologists

Cephalopod morphology for sedimentologists

Brachiopod morphology for sedimentologists

Echinoderm morphology for sedimentologists

Coral morphology for sedimentologists

Graptolite morphology for sedimentologists

 

Annotated images of outcrops, illustrating common sedimentary structures

Sedimentary structures: Shallow marine

Sedimentary structures: Turbidites

Sedimentary structures: Mass transport deposits

Sedimentary structures: Fine-grained fluvial

Sedimentary structures: coarse-grained fluvial

Sedimentary structures: Alluvial fans

Sedimentary structures: Stromatolites

 

Sandstone lithofacies

Sedimentary lithofacies – An introduction

Ripple lithofacies: Ubiquitous bedforms

Climbing ripple lithofacies

Ripple lithofacies influenced by tides

Tabular and trough crossbed lithofacies

Laminated sandstone lithofacies

Low-angle crossbedded sandstone

Hummocky and swaley cross-stratification

Antidune lithofacies

Lithofacies beyond supercritical antidunes

Subaqueous dunes influenced by tides

The three pycnals: Hypo-, homo-, and hyper

Storms and storm surges: Forces at play

Graded-bedding lithofacies

Gravel lithofacies

Introducing coarse-grained lithofacies

Crossbedded gravel lithofacies

Beach and shoreface gravels

Debris flow lithofacies

The lithofacies of mountain streams

 

Three posts on tempestites:

3 Evolving tempestite lithofacies models

2 Storm surges and tempestites

1 Storms and storm surges: Forces at play

 

Seagrass, mangrove, and salt marsh lithofacies

Seagrass meadows and ecosystems

Seagrass lithofacies in the rock record

Mangrove ecosystems

Mangrove lithofacies

Salt marsh lithofacies

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Conjugate fractures and en echelon tension gashes – indicators of brittle failure in Old Red Sandstone, Gougane Barra, County Cork, Ireland.
Mohr-Coulomb failure criteria
A montage of stress transformation paraphernalia and rock deformation
Mohr circles and stress transformation
The Marlborough strike-slip fault array extends north from the dextral Alpine Fault transform; faults continue across Cook Strait to join the North Island Dextral Fault Belt in the Wellington region (central Aotearoa New Zealand). In Marlborough and beneath Cook Strait there are several pull-apart basins formed at releasing bend stepovers. Sandbox analogue models can help us decipher the mechanical and kinematic processes that produce structures like these. Base image from NASA – International Space Station 2003.
Strike-slip analogue models
Scaled sand-box experiments are an ideal medium to observe rock deformation that, in this example, involves synkinematic deposition during rift-like crustal extension. The choice of model materials, in addition to imposed boundary conditions such as strain rates, will determine the outcome of the experiment. Dry sand was chosen for this model because its brittle behaviour under the model conditions is a good representation of natural rock failure. Diagram modified slightly from Eisenstadt and Sims, 2005, Figure 3a.
Analogue structure models: Scaling the materials
The relationship between inertial and gravitational forces expressed by the Froude number (Fr) is reflected by the changes in surface flows and the formation-decay of stationary (standing) waves. Fr < 1 reflects subcritical (tranquil) flow; Fr>1 supercritical flow. Although the Froude number can be determined experimentally, it can also be eased out of a dimensional analysis of the relevant hydrodynamic variables.
Model dimensions and dimensional analysis
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