Mechanical weathering involves breakdown of the rock into particles without altering the chemical composition of the minerals it contains. Ice is the most important agent of mechanical weathering. Water percolates into cracks and fissures within the rock, freezes, and expands. The force exerted by the expansion is sufficient to widen cracks and break off pieces of rock. Heating and cooling of the rock, with its accompanying expansion and contraction, also aid the process. Mechanical weathering contributes to further breakdown of the rock by increasing the surface area exposed to chemical agents.
Chemical weathering corresponds to breakdown of the rock by chemical reaction. This process dissolves some minerals and converts others into particles that can be readily carried away. Air and water are both involved in many complex chemical reactions. Igneous rocks are commonly attacked by water, particularly acid or alkaline solutions, and all the common igneous rock-forming minerals (except quartz, which is very resistant) are changed in this way into clay minerals and chemicals in solution.
The weathered particles-in the form of clay, silt, sand, and gravel- and dissolved materials are transported by water, ice, and wind. These agents reduce the size of the particles, sort them by size, and deposit them at new locations, generally at lower elevation. The sediments dropped by streams and rivers form alluvial fans, flood plains, and deltas, or they reach the bottom of lakes and the sea floor. The wind may move large amounts of sand and other smaller particles. Glaciers transport and deposit great quantities of usually unsorted rock material as till.
As the sediment builds up, the overburden (or “lithostatic”) pressure squeezes it into layered solids in a process known as lithification (rock formation), and the original fluids are expelled. The term “diagenesis” is used to describe all the chemical, physical, and biological changes, including cementation, undergone by a sediment after its initial deposition and during and after its lithification, exclusive of surface weathering.
Sedimentary rocks are laid down in horizontal layers called beds or strata. Each new layer settles above older ones, in a process called superposition. There are usually some gaps in the sequence called unconformities. These represent periods in which no new sediments were laid down, or when earlier sedimentary layers were raised above sea level and eroded away.
Clastic sedimentary rocks
When the particles derived from earlier rocks become deposited, compacted, and cemented together, they form clastic sedimentary rocks. These rocks contain inert minerals that are resistant to mechanical and chemical breakdown, such as quartz, zircon, rutile, and magnetite. Quartz is one of the most resistant minerals, mechanically and chemically.
Sizes of clastic sedimentary rocks
Clastic sedimentary rocks may be regarded as falling along a scale of grain size. Shale is the finest, with particles less than 0.004 millimeters; siltstone is a little bigger, with particles between 0.004 and 0.06 millimeters; sandstone is coarser still, with grains of 0.06 to 2 millimeters; and conglomerates and breccias are the coarsest, with grains 2 to 256 millimeters. Breccia has sharper particles, while conglomerate is categorized by its rounded particles. Arenite is a general term for sedimentary rock with sand-sized particles.
The classification of clastic sedimentary rocks is complex because many variables are involved. The size (or range of sizes) and composition of the particles, the cement, and the matrix (that is, the smaller particles between the larger grains) must all be taken into consideration. Shales, which consist mostly of clay minerals, are generally further classified on the basis of composition and bedding.
Coarser clastic sedimentary rocks are classified according to their particle size and composition. Orthoquartzite is a very pure quartz sandstone; arkose is a sandstone with quartz and abundant feldspar; greywacke is a sandstone with quartz, clay, feldspar, and metamorphic rock fragments present, formed from sediments carried by turbidity currents.
Biochemical sedimentary rocks
Biochemical (or biogenic) sedimentary rocks include carbonate minerals generated by organisms such as corals, molluscs, and foraminifera. Minerals such as calcite (calcium carbonate) cover the ocean floor and later form limestone. Other examples include stromatolites, the flint nodules in chalk (which is itself a biochemical sedimentary rock, a form of limestone), and coal (derived from the remains of tropical plants subjected to high pressure).
Chemical precipitate sedimentary rocks
Chemical precipitate sedimentary rocks are formed when mineral solutions, such as sea water, evaporate. Examples include the evaporite minerals halite and gypsum.
Significance of sedimentary rocks
Sedimentary rocks contain important information about the history of the Earth. They contain fossils, the preserved remains of ancient plants and animals. The composition of sediments provides us with clues about the original rock. Differences between successive layers indicate changes to the environment that have occurred over time. Sedimentary rocks can contain fossils because, unlike most igneous and metamorphic rocks, they form at temperatures and pressures that do not destroy fossil remnants.
The sedimentary rock cover of the continents of the Earth's crust is extensive, but the total contribution of sedimentary rocks is estimated to be only five percent of the total. As such, the sedimentary sequences we see represent only a thin veneer over a crust consisting mainly of igneous and metamorphic rocks.
Sedimentary rocks are also significant in economic terms. Being relatively soft and easy to cut, they are often used as construction material. For example, the White House in Washington, D.C., is made of sandstone. In addition, sedimentary rocks often form porous and permeable reservoirs in sedimentary basins in which petroleum and other hydrocarbons are found.
- Bituminous rock
- Igneous rock
- Metamorphic rock
- Rock (geology)
- Blatt, Harvey, and Robert J. Tracy. 1995. Petrology: Igneous, Sedimentary, and Metamorphic, 2nd ed. New York: W.H. Freeman. ISBN 0716724383
- Farndon, John. 2006. The Practical Encyclopedia of Rocks & Minerals: How to Find, Identify, Collect and Maintain the World's best Specimens, with over 1000 Photographs and Artworks. London: Lorenz Books. ISBN 0754815412
- Pellant, Chris. 2002. Rocks and Minerals. Smithsonian Handbooks. New York: Dorling Kindersley. ISBN 0789491060
- Shaffer, Paul R., Herbert S. Zim, and Raymond Perlman. 2001. Rocks, Gems and Minerals. Rev. ed. New York: St. Martin's Press. ISBN 1582381321
- Skinner, Brian J., Stephen C. Porter, and Jeffrey Park. 2004. Dynamic Earth: An Introduction to Physical Geology. 5th ed. Hoboken, NJ: John Wiley. ISBN 0471152285
- Tucker, Maurice E. 2001. Sedimentary Petrology. 3rd ed. Oxford: Blackwell Publishing. ISBN 0632057351
All links retrieved November 2, 2019.
- A Basic Sedimentary Rock Classification
- PETDB: Petrological Database of the Ocean Floor - Center for International Earth Science Information Network (CIESIN), Columbia University