In geology, a bed is a layer of sediment, sedimentary rock, or volcanic rock "bounded above and below by more or less well-defined bedding surfaces".[1] Specifically in sedimentology, a bed can be defined in one of two major ways.[2] First, Campbell[3] and Reineck and Singh[4] use the term bed to refer to a thickness-independent layer comprising a coherent layer of sedimentary rock, sediment, or pyroclastic material bounded above and below by surfaces known as bedding planes. By this definition of bed, laminae are small beds that constitute the smallest (visible) layers of a hierarchical succession and often, but not always, internally comprise a bed.[2]
Alternatively, a bed can be defined by thickness where a bed is a coherent layer of sedimentary rock, sediment, or pyroclastic material greater than 1 cm thick and a lamina is a coherent layer of sedimentary rock, sediment, or pyroclastic material less than 1 cm thick.[5] This method of defining bed versus lamina is frequently used in textbooks, e.g., Collinson & Mountney[6] or Miall.[7] Both definitions have merit and the choice of which one to use will depend on the focus of the specific study on a case by case basis.[2]
In geology, a bedding surface is either a planar, nearly planar, to wavy or curved 3-dimensional surface that visibly separates each successive bed (of the same or different lithology) from the preceding or following bed. Where bedding surfaces occur as cross-sections, e.g., in a 2-dimensional vertical cliff face of horizontal strata, are often referred to as bedding contacts. Within conformable successions, each bedding surface acted as the depositional surface for the accumulation of younger sediment.[1] [2]
Typically, but not always, bedding surfaces record changes in either the rate or type of accumulating sediment that created the underlying bed. Typically, they represent either a period of nondeposition, erosional truncation, shift in flow or sediment regime, abrupt change in composition, or combination of these as a result of changes in environmental conditions. As a result, a bed is typically, but not always, interpreted to represent a single period of time when sediments or pyroclastic material accumulated during uniform and steady paleoenvironmental conditions. However, some bedding surfaces may be postdepositional features either formed or enhanced by diagenetic processes or weathering.[2] [8]
The relationship between bedding surfaces controls the gross geometry of a bed. Most commonly, the bottom and top surfaces of beds are subparallel to parallel to each other. However, some bedding surfaces of a bed are nonparallel, e.g., wavy, or curved. Differing combinations of nonparallel bedding surfaces results in beds of widely varying geometric shapes such as uniform-tabular, tabular-lenticular, curved-tabular, wedge-shaped, and irregular beds.[9]
Types of beds include cross-beds and graded beds. Cross-beds, or "sets," are not layered horizontally and are formed by a combination of local deposition on the inclined surfaces of ripples or dunes, and local erosion. Graded beds show a gradual change in grain or clast sizes from one side of the bed to the other. A normal grading occurs where there are larger grain sizes on the older side, while an inverse grading occurs where there are smaller grain sizes on the older side.[4] [6] [9]
Bed thickness is a basic and important characteristic of beds. Besides mapping stratigraphic units and interpreting sedimentary facies, the analysis of bed thickness can be used to recognize breaks in sedimentation, cyclic sedimentation patterns, and gradual environmental changes.[10] Such sedimentological studies are typically based on the hypothesis that the thicknesses of stratigraphic units follows a lognormal distribution.[10] [11] Differing nomenclatures for the bed and laminae thickness have been proposed by various authors, including McKee and Weir,[5] Ingram,[12] and Reineck and Singh.[4] However, none of them have been universally accepted by Earth scientists.[10] [13] In the practice of engineering geology, a standardized nomenclature is used for describing bed thickness in Australia,[14] European Union,[15] and United Kingdom.[16]
Examples of widely used bed thickness classifications include Tucker (1982)[17] and McKee and Weir[5] (1953).
| Very thick | > 1 m | > 120 cm | |
| Thick | 30 cm – 1 m | 60–120 cm | |
| Medium | 10 – 30 cm | ||
| Thin | 3 – 10 cm | 5–60 cm | |
| Very thin | 1 – 3 cm | 1–5 cm | |
| Thickly laminated | 3 – 10 mm | 2 mm - 1 cm | |
| Thinly laminated | < 3 mm | < 2 mm |
According to both the North American Stratigraphic Code and International Stratigraphic Guide, a bed is the smallest formal lithostratigraphic unit that can be used for sedimentary rocks. A bed, a stratum, is the smallest formal unit in the hierarchy of sedimentary lithostratigraphic units and is lithologically distinguishable from other layers above and below. Customarily, only distinctive beds, i.e. key beds, marker beds, that are particularly useful for stratigraphic purposes are given proper names and considered formal lithostratigraphic units.[18] [19]
In case of volcanic rocks, the lithostratigraphic unit equivalent to a bed is a flow. A flow is “...a discrete, extrusive, volcanic rock body distinguishable by texture, composition, order of superposition, paleomagnetism, or other objective criteria.” A flow is a part of a member as a bed of sedimentary rock is a part of a member.[18] [19]
In geotechnical engineering a bedding surface often forms a discontinuity that may have a large influence on the mechanical behaviour (strength, deformation, etc.) of soil and rock masses in tunnel, foundation, or slope construction.
See main article: Relative dating. These are the principles which apply to all geologic features, and can be used to describe the order of events in a feature's geologic history.