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Igneous rock
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Geologic provinces of the World (USGS)
Shield
Platform
Orogen
Basin
Large igneous province
Extended crust
Oceanic crust:
0–20 Ma
20–65 Ma
>65 Ma
Igneous rock (derived from the Latin word ignis meaning fire), or magmatic rock, is one of the three main rock types, the others being sedimentary and metamorphic. Igneous rock is formed through the cooling and solidification of magma or lava. The magma can be derived from partial melts of existing rocks in either a planet's mantle or crust. Typically, the melting is caused by one or more of three processes: an increase in temperature, a decrease in pressure, or a change in composition. Solidification into rock occurs either below the surface as intrusive rocks or on the surface as extrusive rocks. Igneous rock may form with crystallization to form granular, crystalline rocks, or without crystallization to form natural glasses.
Contents
[hide]
1 Geological significance
2 Geological setting
2.1 Intrusive
2.2 Extrusive
3 Classification
3.1 Texture
3.2 Chemical classification and petrology
3.3 History of classification
4 Mineralogical classification
4.1 Example of classification
5 Magma origination
5.1 Decompression
5.2 Effects of water and carbon dioxide
5.3 Temperature increase
5.4 Magma evolution
6 Etymology
7 See also
8 Notes
9 References
10 Additional Reading
11 External links
Geological significance
Igneous and metamorphic rocks make up 90–95% of the top 16 km of the Earth's crust by volume.[1] Igneous rocks form about 15% of the Earth's current land surface.[note 1] Most of the Earth's oceanic crust is made of igneous rock.
Igneous rocks are also geologically important because:
their minerals and global chemistry give information about the composition of the mantle, from which some igneous rocks are extracted, and the temperature and pressure conditions that allowed this extraction, and/or of other pre-existing rock that melted;
their absolute ages can be obtained from various forms of radiometric dating and thus can be compared to adjacent geological strata, allowing a time sequence of events;
their features are usually characteristic of a specific tectonic environment, allowing tectonic reconstitutions (see plate tectonics);
in some special circumstances they host important mineral deposits (ores): for example, tungsten, tin, and uranium are commonly associated with granites and diorites, whereas ores of chromium and platinum are commonly associated with gabbros.
Geological setting
Forming of igneous rock
In terms of modes of occurrence, igneous rocks can be either intrusive (plutonic and hypabyssal) or extrusive (volcanic).
Intrusive
Close-up of granite (an intrusive igneous rock) exposed in Chennai, India.
Intrusive igneous rocks are formed from magma that cools and solidifies within the crust of a planet, surrounded by pre-existing rock (called country rock); the magma cools slowly and, as a result, these rocks are coarse-grained. The mineral grains in such rocks can generally be identified with the naked eye. Intrusive rocks can also be classified according to the shape and size of the intrusive body and its relation to the other formations into which it intrudes. Typical intrusive formations are batholiths, stocks, laccoliths, sills and dikes. When the magma solidifies within the earth's crust, it cools slowly forming coarse textured rocks, such as granite, gabbro, or diorite.
The central cores of major mountain ranges consist of intrusive igneous rocks, usually granite. When exposed by erosion, these cores (called batholiths) may occupy huge areas of the Earth's surface.
Intrusive igneous rocks that form at depth within the crust are termed plutonic (or abyssal) rocks and are usually coarse-grained. Intrusive igneous rocks that form near the surface are termed subvolcanic or hypabyssal rocks and they are usually medium-grained. Hypabyssal rocks are less common than plutonic or volcanic rocks and often form dikes, sills, laccoliths, lopoliths, or phacoliths.
Extrusive
Extrusive igneous rock is made from lava released by volcanoes
Sample of basalt (an extrusive igneous rock), found in Massachusetts
Extrusive igneous rocks, also known as volcanic rocks, are formed at the crust's surface as a result of the partial melting of rocks within the mantle and crust. Extrusive igneous rocks cool and solidify quicker than intrusive igneous rocks. They are formed by the cooling of molten magma on the earth's surface. The magma, which is brought to the surface through fissures or volcanic eruptions, solidifies at a faster rate. Hence such rocks are smooth, crystalline and fine-grained. Basalt is a common extrusive igneous rock and forms lava flows, lava sheets and lava plateaus. Some kinds of basalt solidify to form long polygonal columns. The Giant's Causeway in Antrim, Northern Ireland is an example.
The molten rock, with or without suspended crystals and gas bubbles, is called magma. It rises because it is less dense than the rock from which it was created. When magma reaches the surface from beneath water or air, it is called lava. Eruptions of volcanoes into air are termed subaerial, whereas those occurring underneath the ocean are termed submarine. Black smokers and mid-ocean ridge basalt are examples of submarine volcanic activity.
The volume of extrusive rock erupted annually by volcanoes varies with plate tectonic setting. Extrusive rock is produced in the following proportions:[3]
divergent boundary: 73%
convergent boundary (subduction zone): 15%
hotspot: 12%.
Magma that erupts from a volcano behaves according to its viscosity, determined by temperature, composition, crystal content and the amount of silica. High-temperature magma, most of which is basaltic in composition, behaves in a manner similar to thick oil and, as it cools, treacle. Long, thin basalt flows with pahoehoe surfaces are common. Intermediate composition magma, such as andesite, tends to form cinder cones of intermingled ash, tuff and lava, and may have a viscosity similar to thick, cold molasses or even rubber when erupted. Felsic magma, such as rhyolite, is usually erupted at low temperature and is up to 10,000 times as viscous as basalt. Volcanoes with rhyolitic magma commonly erupt explosively, and rhyolitic lava flows are typically of limited extent and have steep margins, because the magma is so viscous.
Felsic and intermediate magmas that erupt often do so violently, with explosions driven by the release of dissolved gases—typically water vapour, but also carbon dioxide. Explosively erupted pyroclastic material is called tephra and includes tuff, agglomerate and ignimbrite. Fine volcanic ash is also erupted and forms ash tuff deposits, which can often cover vast areas.
Because lava usually cools and crystallizes rapidly, it is usually fine-grained. If the cooling has been so rapid as to prevent the formation of even small crystals after extrusion, the resulting rock may be mostly glass (such as the rock obsidian). If the cooling of the lava happened more slowly, the rock would be coarse-grained.
Because the minerals are mostly fine-grained, it is much more difficult to distinguish between the different types of extrusive igneous rocks than between different types of intrusive igneous rocks. Generally, the mineral constituents of fine-grained extrusive igneous rocks can only be determined by examination of thin sections of the rock under a microscope, so only an approximate classification can usually be made in the field.
Classification
Igneous rocks are classified according to mode of occurrence, texture, mineralogy, chemical composition, and the geometry of the igneous body.
The classification of the many types of different igneous rocks can provide us with important information about the conditions under which they formed. Two important variables used for the classification of igneous rocks are particle size, which largely depends on the cooling history, and the mineral composition of the rock. Feldspars, quartz or feldspathoids, olivines, pyroxenes, amphiboles, and micas are all important minerals in the formation of almost all igneous rocks, and they are basic to the classification of these rocks. All other minerals present are regarded as nonessential in almost all igneous rocks and are called accessory minerals. Types of igneous rocks with other essential minerals are very rare, and these rare rocks include those with essential carbonates.
In a simplified classification, igneous rock types are separated on the basis of the type of feldspar present, the presence or absence of quartz, and in rocks with no feldspar or quartz, the type of iron or magnesium minerals present. Rocks containing quartz (silica in composition) are silica-oversaturated. Rocks with feldspathoids are silica-undersaturated, because feldspathoids cannot coexist in a stable association with quartz.
Igneous rocks that have crystals large enough to be seen by the naked eye are called phaneritic; those with crystals too small to be seen are called aphanitic. Generally speaking, phaneritic implies an intrusive origin; aphanitic an extrusive one.
An igneous rock with larger, clearly discernible crystals embedded in a finer-grained matrix is termed porphyry. Porphyritic texture develops when some of the crystals grow to considerable size before the main mass of the magma crystallizes as finer-grained, uniform material.
Igneous rocks are classified on the basis of texture and composition. Texture refers to the size, shape, and arrangement of the mineral grains or crystals of which the rock is composed.
Texture
Gabbro specimen showing phaneritic texture; Rock Creek Canyon, eastern Sierra Nevada, California; scale bar is 2.0 cm.
Main article: Rock microstructure
Texture is an important criterion for the naming of volcanic rocks. The texture of volcanic rocks, including the size, shape, orientation, and distribution of mineral grains and the intergrain relationships, will determine whether the rock is termed a tuff, a pyroclastic lava or a simple lava.
However, the texture is only a subordinate part of classifying volcanic rocks, as most often there needs to be chemical information gleaned from rocks with extremely fine-grained groundmass or from airfall tuffs, which may be formed from volcanic ash.
Textural criteria are less critical in classifying intrusive rocks where the majority of minerals will be visible to the naked eye or at least using a hand lens, magnifying glass or microscope. Plutonic rocks also tend to be less texturally varied and less prone to gaining structural fabrics. Textural terms can be used to differentiate different intrusive phases of large plutons, for instance porphyritic margins to large intrusive bodies, porphyry stocks and subvolcanic dikes (apophyses). Mineralogical classification is most often used to classify plutonic rocks. Chemical classifications are preferred to classify volcanic rocks, with phenocryst species used as a prefix, e.g. "olivine-bearing picrite" or "orthoclase-phyric rhyolite".
see also List of rock textures and Igneous textures
Basic classification scheme for igneous rocks on their mineralogy. If the approximate volume fractions of minerals in the rock are known, the rock name and silica content can be read off the diagram. This is not an exact method, because the classification of igneous rocks also depends on other components than silica, yet in most cases it is a good first guess.
Chemical classification and petrology
Total alkali versus silica classification scheme (TAS) as proposed in Le Maitre's 2002 Igneous Rocks - A classification and glossary of terms[4]:237
Igneous rocks can be classified according to chemical or mineralogical parameters.
Chemical: total alkali-silica content (TAS diagram) for volcanic rock classification used when modal or mineralogic data is unavailable:
felsic igneous rocks containing a high silica content, greater than 63% SiO2 (examples granite and rhyolite),
intermediate igneous rocks containing between 52–63% SiO2 (example andesite and dacite),
mafic igneous rocks have low silica 45–52% and typically high iron – magnesium content (example gabbro and basalt),
ultramafic rock igneous rocks with less than 45% silica (examples picrite, komatiite and peridotite),
alkalic igneous rocks with 5–15% alkali (K2O + Na2O) content or with a molar ratio of alkali to silica greater than 1:6 (examples phonolite and trachyte).
Chemical classification also extends to differentiating rocks that are chemically similar according to the TAS diagram, for instance:
Ultrapotassic – rocks containing molar K2O/Na2O >3.
Peralkaline – rocks containing molar (K2O + Na2O)/Al2O3 >1.
Peraluminous – rocks containing molar (K2O + Na2O)/Al2O3 <1.
An idealized mineralogy (the normative mineralogy) can be calculated from the chemical composition, and the calculation is useful for rocks too fine-grained or too altered for identification of minerals that crystallized from the melt. For instance, normative quartz classifies a rock as silica-oversaturated; an example is rhyolite. In an older terminology, silica oversaturated rocks were called silicic or acidic where the SiO2 was greater than 66% and the family term quartzolite was applied to the most silicic. A normative feldspathoid classifies a rock as silica-undersaturated; an example is nephelinite.
History of classification
In 1902, a group of American petrographers proposed that all existing classifications of igneous rocks should be discarded and replaced by a "quantitative" classification based on chemical analysis. They showed how vague, and often unscientific, much of the existing terminology was and argued that as the chemical composition of an igneous rock was its most fundamental characteristic, it should be elevated to prime position.
Geological occurrence, structure, mineralogical constitution—the hitherto accepted criteria for the discrimination of rock species—were relegated to the background. The completed rock analysis is first to be interpreted in terms of the rock-forming minerals which might be expected to be formed when the magma crystallizes, e.g., quartz feldspars, olivine, akermannite, Feldspathoids, magnetite, corundum, and so on, and the rocks are divided into groups strictly according to the relative proportion of these minerals to one another.[5][6]
Mineralogical classification
For volcanic rocks, mineralogy is important in classifying and naming lavas. The most important criterion is the phenocryst species, followed by the groundmass mineralogy. Often, where the groundmass is aphanitic, chemical classification must be used to properly identify a volcanic rock.
Mineralogic contents – felsic versus mafic
felsic rock, highest content of silicon, with predominance of quartz, alkali feldspar and/or feldspathoids: the felsic minerals; these rocks (e.g., granite, rhyolite) are usually light coloured, and have low density.
mafic rock, lesser content of silicon relative to felsic rocks, with predominance of mafic minerals pyroxenes, olivines and calcic plagioclase; these rocks (example, basalt, gabbro) are usually dark coloured, and have a higher density than felsic rocks.
ultramafic rock, lowest content of silicon, with more than 90% of mafic minerals (e.g., dunite).
For intrusive, plutonic and usually phaneritic igneous rocks (where all minerals are visible at least via microscope), the mineralogy is used to classify the rock. This usually occurs on ternary diagrams, where the relative proportions of three minerals are used to classify the rock.
The following table is a simple subdivision of igneous rocks according to both their composition and mode of occurrence.
Composition
Mode of occurrence
Felsic Intermediate Mafic Ultramafic
Intrusive Granite Diorite Gabbro Peridotite
Extrusive Rhyolite Andesite Basalt Komatiite
For a more detailed classification see QAPF diagram.
Example of classification
Granite is an igneous intrusive rock (crystallized at depth), with felsic composition (rich in silica and predominately quartz plus potassium-rich feldspar plus sodium-rich plagioclase) and phaneritic, subeuhedral texture (minerals are visible to the unaided eye and commonly some of them retain original crystallographic shapes).
Magma origination
The Earth's crust averages about 35 kilometers thick under the continents, but averages only some 7–10 kilometers beneath the oceans. The continental crust is composed primarily of sedimentary rocks resting on a crystalline basement formed of a great variety of metamorphic and igneous rocks, including granulite and granite. Oceanic crust is composed primarily of basalt and gabbro. Both continental and oceanic crust rest on peridotite of the mantle.
Rocks may melt in response to a decrease in pressure, to a change in composition (such as an addition of water), to an increase in temperature, or to a combination of these processes.
Other mechanisms, such as melting from a meteorite impact, are less important today, but impacts during the accretion of the Earth led to extensive melting, and the outer several hundred kilometers of our early Earth was probably an ocean of magma. Impacts of large meteorites in the last few hundred million years have been proposed as one mechanism responsible for the extensive basalt magmatism of several large igneous provinces.
Decompression
Decompression melting occurs because of a decrease in pressure.[7]
The solidus temperatures of most rocks (the temperatures below which they are completely solid) increase with increasing pressure in the absence of water. Peridotite at depth in the Earth's mantle may be hotter than its solidus temperature at some shallower level. If such rock rises during the convection of solid mantle, it will cool slightly as it expands in an adiabatic process, but the cooling is only about 0.3 °C per kilometer. Experimental studies of appropriate peridotite samples document that the solidus temperatures increase by 3 °C to 4 °C per kilometer. If the rock rises far enough, it will begin to melt. Melt droplets can coalesce into larger volumes and be intruded upwards. This process of melting from the upward movement of solid mantle is critical in the evolution of the Earth.
Decompression melting creates the ocean crust at mid-ocean ridges. It also causes volcanism in intraplate regions, such as Europe, Africa and the Pacific sea floor. There, it is variously attributed either to the rise of mantle plumes (the "Plume hypothesis") or to intraplate extension (the "Plate hypothesis").[8]
Effects of water and carbon dioxide
The change of rock composition most responsible for the creation of magma is the addition of water. Water lowers the solidus temperature of rocks at a given pressure. For example, at a depth of about 100 kilometers, peridotite begins to melt near 800 °C in the presence of excess water, but near or above about 1,500 °C in the absence of water.[9] Water is driven out of the oceanic lithosphere in subduction zones, and it causes melting in the overlying mantle. Hydrous magmas composed of basalt and andesite are produced directly and indirectly as results of dehydration during the subduction process. Such magmas, and those derived from them, build up island arcs such as those in the Pacific Ring of Fire. These magmas form rocks of the calc-alkaline series, an important part of the continental crust.
The addition of carbon dioxide is relatively a much less important cause of magma formation than the addition of water, but genesis of some silica-undersaturated magmas has been attributed to the dominance of carbon dioxide over water in their mantle source regions. In the presence of carbon dioxide, experiments document that the peridotite solidus temperature decreases by about 200 °C in a narrow pressure interval at pressures corresponding to a depth of about 70 km. At greater depths, carbon dioxide can have more effect: at depths to about 200 km, the temperatures of initial melting of a carbonated peridotite composition were determined to be 450 °C to 600 °C lower than for the same composition with no carbon dioxide.[10] Magmas of rock types such as nephelinite, carbonatite, and kimberlite are among those that may be generated following an influx of carbon dioxide into mantle at depths greater than about 70 km.
Temperature increase
Increase in temperature is the most typical mechanism for formation of magma within continental crust. Such temperature increases can occur because of the upward intrusion of magma from the mantle. Temperatures can also exceed the solidus of a crustal rock in continental crust thickened by compression at a plate boundary. The plate boundary between the Indian and Asian continental masses provides a well-studied example, as the Tibetan Plateau just north of the boundary has crust about 80 kilometers thick, roughly twice the thickness of normal continental crust. Studies of electrical resistivity deduced from magnetotelluric data have detected a layer that appears to contain silicate melt and that stretches for at least 1,000 kilometers within the middle crust along the southern margin of the Tibetan Plateau.[11] Granite and rhyolite are types of igneous rock commonly interpreted as products of the melting of continental crust because of increases in temperature. Temperature increases also may contribute to the melting of lithosphere dragged down in a subduction zone.
Magma evolution
Schematic diagrams showing the principles behind fractional crystallisation in a magma. While cooling, the magma evolves in composition because different minerals crystallize from the melt. 1: olivine crystallizes; 2: olivine and pyroxene crystallize; 3: pyroxene and plagioclase crystallize; 4: plagioclase crystallizes. At the bottom of the magma reservoir, a cumulate rock forms.
Main article: Igneous differentiation
Most magmas only entirely melt for small parts of their histories. More typically, they are mixes of melt and crystals, and sometimes also of gas bubbles. Melt, crystals, and bubbles usually have different densities, and so they can separate as magmas evolve.
As magma cools, minerals typically crystallize from the melt at different temperatures (fractional crystallization). As minerals crystallize, the composition of the residual melt typically changes. If crystals separate from the melt, then the residual melt will differ in composition from the parent magma. For instance, a magma of gabbroic composition can produce a residual melt of granitic composition if early formed crystals are separated from the magma. Gabbro may have a liquidus temperature near 1,200 °C, and the derivative granite-composition melt may have a liquidus temperature as low as about 700 °C. Incompatible elements are concentrated in the last residues of magma during fractional crystallization and in the first melts produced during partial melting: either process can form the magma that crystallizes to pegmatite, a rock type commonly enriched in incompatible elements. Bowen's reaction series is important for understanding the idealised sequence of fractional crystallisation of a magma.
Magma composition can be determined by processes other than partial melting and fractional crystallization. For instance, magmas commonly interact with rocks they intrude, both by melting those rocks and by reacting with them. Magmas of different compositions can mix with one another. In rare cases, melts can separate into two immiscible melts of contrasting compositions.
There are relatively few minerals that are important in the formation of common igneous rocks, because the magma from which the minerals crystallize is rich in only certain elements: silicon, oxygen, aluminium, sodium, potassium, calcium, iron, and magnesium. These are the elements that combine to form the silicate minerals, which account for over ninety percent of all igneous rocks. The chemistry of igneous rocks is expressed differently for major and minor elements and for trace elements. Contents of major and minor elements are conventionally expressed as weight percent oxides (e.g., 51% SiO2, and 1.50% TiO2). Abundances of trace elements are conventionally expressed as parts per million by weight (e.g., 420 ppm Ni, and 5.1 ppm Sm). The term "trace element" is typically used for elements present in most rocks at abundances less than 100 ppm or so, but some trace elements may be present in some rocks at abundances exceeding 1,000 ppm. The diversity of rock compositions has been defined by a huge mass of analytical data—over 230,000 rock analyses can be accessed on the web through a site sponsored by the U. S. National Science Foundation (see the External Link to EarthChem).
Etymology
The word "igneous" is derived from the Latin ignis, meaning "of fire". Volcanic rocks are named after Vulcan, the Roman name for the god of fire. Intrusive rocks are also called "plutonic" rocks, named after Pluto, the Roman god of the underworld.
See also
Large igneous province
List of rock types
Metamorphic rock
Migmatite
Petrology
Sedimentary rock
Notes
Jump up ^ 15% is the arithmetic sum of the area for intrusive plutonic rock (7%) plus the area for extrusive volcanic rock (8%).[2]
References
Jump up ^ Prothero, Donald R.; Schwab, Fred (2004). Sedimentary geology : an introduction to sedimentary rocks and stratigraphy (2nd ed.). New York: Freeman. p. 12. ISBN 978-0-7167-3905-0.
Jump up ^ Wilkinson, Bruce H.; McElroy, Brandon J.; Kesler, Stephen E.; Peters, Shanan E.; Rothman, Edward D. (2008). "Global geologic maps are tectonic speedometers—Rates of rock cycling from area-age frequencies". Geological Society of America Bulletin. 121 (5–6): 760–779. doi:10.1130/B26457.1.
Jump up ^ Fisher, R. V. & Schmincke H.-U., (1984) Pyroclastic Rocks, Berlin, Springer-Verlag
Jump up ^ Ridley, W. I., 2012, Petrology of Igneous Rocks, Volcanogenic Massive Sulfide Occurrence Model, USGS Scientific Report 2010-5070-C, Chapter 15.
Jump up ^ Cross, W. et al. (1903) Quantitative Classification of Igneous Rocks, Chicago, University of Chicago Press
Jump up ^ One or more of the preceding sentences incorporates text from a publication now in the public domain: Chisholm, Hugh, ed. (1911). "Petrology". Encyclopædia Britannica. 21 (11th ed.). Cambridge University Press. pp. 323–333.
Jump up ^ Geoff C. Brown; C. J. Hawkesworth; R. C. L. Wilson (1992). Understanding the Earth (2nd ed.). Cambridge University Press. p. 93. ISBN 0-521-42740-1.
Jump up ^ Foulger, G.R. (2010). Plates vs. Plumes: A Geological Controversy. Wiley-Blackwell. ISBN 978-1-4051-6148-0.
Jump up ^ T. L. Grove, N. Chatterjee, S. W. Parman, and E. Medard, (2006)The influence of H2O on mantle wedge melting. Earth and Planetary Science Letters, v. 249, p. 74-89
Jump up ^ R. Dasgupta and M. M. Hirschmann (2007) Effect of variable carbonate concentration on the solidus of mantle peridotite. American Mineralogist, v. 92, p. 370-379
Jump up ^ M. J. Unsworth et al. (2005) Crustal rheology of the Himalaya and Southern Tibet inferred from magnetotelluric data. Nature, v. 438, p. 78-81
Additional Reading
R. W. Le Maitre (editor) (2002) Igneous Rocks: A Classification and Glossary of Terms, Recommendations of the International Union of Geological Sciences, Subcommission of the Systematics of Igneous Rocks., Cambridge, Cambridge University Press ISBN 0-521-66215-X
External links
The Wikibook Historical Geology has a page on the topic of: Igneous rocks and stratigraphy
The Wikibook Historical Geology has a page on the topic of: Igneous rocks
USGS Igneous Rocks
Igneous rock classification flowchart
Igneous Rocks Tour, an introduction to Igneous Rocks
The IUGS systematics of igneous rocks
Wikimedia Commons has media related to Igneous rocks.
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Common igneous rocks classified by silicon dioxide content
Type Ultramafic
<45% SiO2 Mafic
45–52% SiO2 Intermediate
52–63% SiO2 Intermediate–felsic
63–69% SiO2 Felsic
>69% SiO2
Volcanic rocks:
Subvolcanic rocks:
Plutonic rocks:
Komatiite, Picrite basalt
Kimberlite, Lamproite
Peridotite
Basalt
Diabase (Dolerite)
Gabbro
Andesite
Microdiorite
Diorite
Dacite
Microgranodiorite
Granodiorite
Rhyolite
Microgranite, Aplite
Granite
Authority control
GND: 4036974-2
NDL: 00565095
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Ann B. Davis
From Wikipedia, the free encyclopedia
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Ann B. Davis
Ann B. Davis, c. 1973
Born
Ann Bradford Davis
(1926-05-03)May 3, 1926
Schenectady, New York, U.S.
Died
June 1, 2014(2014-06-01) (aged 88)
San Antonio, Texas, U.S.
Cause of death
Subdural hematoma
Alma mater
University of Michigan
Occupation
Actress
Years active
1953–1997
Known for
The Bob Cummings Show
The Brady Bunch
Ann Bradford Davis (May 3, 1926 – June 1, 2014) was an American actress.[1][2] She achieved prominence for her role in the NBC situation comedy The Bob Cummings Show (1955–1959), for which she twice won the Primetime Emmy Award for Outstanding Supporting Actress in a Comedy Series, but she was best known for playing the part of Alice Nelson, the housekeeper in ABC's The Brady Bunch (1969–1974).
Contents
[hide]
1 Early life
2 Career
3 Personal life
4 Death
5 Works
5.1 Film
5.2 Television
5.3 Stage
6 Awards and nominations
7 References
8 External links
Early life
Davis was born in Schenectady, New York, the daughter of Marguerite (née Stott) and Cassius Miles Davis.[1] She had an identical twin, Harriet, and an older brother, Evans.[3][4] When she was three, she and her family moved to Erie in northwestern Pennsylvania.[2] She graduated from Strong Vincent High School and later from the University of Michigan in Ann Arbor.[5] She originally enrolled as a pre-medical major; however, she changed her mind and went into drama after seeing her older brother's performance of Oklahoma![2] Davis graduated in 1948 with a degree in drama and speech.[2]
Career
Davis with Bob Cummings on The Bob Cummings Show, 1958
Davis' most famous role was as housekeeper Alice Nelson on the classic 70s sitcom The Brady Bunch.
In the 1953–1954 season, Davis appeared as a musical judge on ABC's Jukebox Jury.[6]
Davis's first television success was as Charmaine "Schultzy" Schultz in The Bob Cummings Show, 1955-1959.[7] She auditioned for the role, because her friend's boyfriend was a casting director and recommended her for the part.[2] She won the Primetime Emmy Award for Outstanding Supporting Actress in a Comedy Series twice out of four nominations for this role.[7]
She appeared on January 23, 1958, as a guest star on The Ford Show, Starring Tennessee Ernie Ford. On February 9, 1960, Davis received a star on the Hollywood Walk of Fame.[8]
In the 1965–1966 television season, Davis appeared as Miss Wilson, a physical education teacher at a private girls' academy in John Forsythe's single-season NBC sitcom, The John Forsythe Show.[9]
For a period in the 1960s and 1970s, Davis was known for her appearances in television commercials for the Ford Motor Company, particularly for the mid-sized Ford Fairlane models. Davis was also featured in commercials for Minute Rice in Canada until the mid-1980s.
From 1969 to 1974, Davis played housekeeper Alice Nelson in The Brady Bunch television series. She later returned to take part in various Brady Bunch television movies, including The Brady Girls Get Married (1981) and A Very Brady Christmas (1988). She also reprised her role as Alice Nelson in two short-lived Brady Bunch spin-off television series: The Brady Brides (1981) and The Bradys (1990), both of which lasted only six episodes. She also made a cameo appearance as a truck driver named "Schultzy", a reference to her days on The Bob Cummings Show, in The Brady Bunch Movie in 1995. In 1994, Davis published a cookbook, Alice's Brady Bunch Cookbook, with Brady Bunch inspired recipes.[10] The book also includes recipes from cast members.[11]
In the early 1990s, Davis focused on theater. She performed in a production of Arsenic and Old Lace, and a world tour production of Crazy for You.[12]
Davis never completely retired from acting; in her later years she was the celebrity spokeswoman in several Shake 'n Bake commercials, and later appeared in several disposable mop commercials for Swiffer.[3][13] She also appeared in a number of Brady Bunch reunion projects, most recently TV Land's The Brady Bunch 35th Anniversary Reunion Special: Still Brady After All These Years. On April 22, 2007, The Brady Bunch was awarded the TV Land Pop Culture Award on the 5th annual TV Land Awards. Davis and other cast members accepted the award, and she received a standing ovation.[citation needed]
Personal life
Davis in November 2007
In 1976, Davis sold her home in Los Angeles to move to Denver, Colorado, where she joined an Episcopal community led by Bishop William C. Frey.[14] The community later relocated to Ambridge in Beaver County in far western Pennsylvania after Frey became dean of the seminary Trinity School for Ministry.[2] Davis had long been a volunteer for the Episcopal Church, working at the General Convention,[15] attending services at churches around the country.[14]
Davis never married nor was she publicly known to have been romantically linked to anyone.[16]
Death
Davis died at the age of 88 on June 1, 2014, at a hospital in San Antonio, Texas. Earlier in the day, she had sustained a subdural hematoma from a fall in her bathroom in the San Antonio residence, in which she lived with Bishop Frey and his wife, Barbara.[17][18][19] Sources close to her say she was in excellent health for a woman her age, and her death was a complete shock.[20] She is buried in the Saint Helena's Columbarium and Memorial Gardens in Boerne, Kendall County, Texas.[21]
Works
This section needs additional citations for verification. Please help improve this article by adding citations to reliable sources. Unsourced material may be challenged and removed. (June 2014) (Learn how and when to remove this template message)
Film
Year
Title
Role
Notes
1955 A Man Called Peter[22] Ruby Coleman Uncredited
1956 The Best Things in Life Are Free Hattie Stewart Uncredited
1960 Pepe[22] Ann B. "Schultzy" Davis
1961 All Hands on Deck[22] Nobby
1961 Lover Come Back Millie
1994 Naked Gun 33⅓: The Final Insult Alice Nelson Credited as playing herself
1995 The Brady Bunch Movie Trucker (Shultzy)
Television
Year
Title
Role
Notes
1953–1953 Jukebox Jury Herself/Judge Musical series
1956 Matinee Theater Peg Miller Episode: "Belong to Me"
1956 Lux Video Theatre Miss Killicat Episode: "The Wayward Saint"
1955–1959 The Bob Cummings Show Charmaine "Schultzy" Schultz 153 episodes
1960 Wagon Train[23] Mrs. Foster Episode: "The Countess Baranof Story"
1962 The New Breed Elizabeth MacBaine Episode: "Wherefore Art Thou, Romeo?"
1962 Here's Hollywood Herself Celebrity interview program
1963 McKeever and the Colonel Sgt. Gruber Episode: "Too Many Sergeants"
1963 The Keefe Brasselle Show[24] Herself 3 appearances on summer replacement series for The Garry Moore Show
1964 Bob Hope Presents the Chrysler Theatre Matha Episode: "Wake Up, Darling"
1965–1966 The John Forsythe Show Miss Wilson 29 episodes
1966 The Pruitts of Southampton Mrs. Derwin Episode: "Phyllis Takes a Letter"
1968 Insight Pat Episode: "The Late Great God"
1970/1973 Love, American Style[23] 2 episodes
1971 Big Fish, Little Fish Hilda Rose Movie
1973 The World of Sid & Marty Krofft at the Hollywood Bowl Audience member Uncredited
1969–1974 The Brady Bunch Alice Nelson / Cousin Emma 117 episodes
1974 Only with Married Men Mola Movie; uncredited
1976–1977 The Brady Bunch Hour Alice Nelson 9 episodes
1980 The Love Boat[23] Agnes Episode: "Invisible Maniac/September Song/Peekaboo"
1981 The Brady Girls Get Married Alice Nelson Movie
1981 The Brady Brides 6 episodes
1988 A Very Brady Christmas Movie
1989 Day by Day[23] Episode: "A Very Brady Episode"
1990 The Bradys 4 episodes
1991 Hi Honey, I'm Home![23] Episode: "SRP"
1997 Something So Right[25] Maxine Episode: "Something About Inter-Ex-Spousal Relations"
Stage
Year
Title
Role
Venue
Notes
1972–1973 No, No, Nanette
1992–1996 Crazy for You Mother
1996 Arsenic and Old Lace Abby Brewster
Awards and nominations
Davis received four Primetime Emmy Award nominations, resulting in two awards, for her portrayal of Charmaine "Schultzy" Schultz on The Bob Cummings Show.
Television Season
Award
Category
Television Program
Result
Notes
1955–1956 Emmy Award Best Actress in a Supporting Role The Bob Cummings Show
(Episode: "Schultzy's Dream World") Nominated Lost to Nanette Fabray (Caesar's Hour)
1956–1957 Emmy Award Best Supporting Performance by an Actress The Bob Cummings Show Nominated Lost to Pat Carroll (Caesar's Hour)
1957–1958 Emmy Award Best Continuing Supporting Performance by an Actress in a Dramatic or Comedy Series The Bob Cummings Show Won
1958–1959 Emmy Award Best Supporting Actress (Continuing Character) in a Comedy Series The Bob Cummings Show Won
On February 9, 1960, Davis also received a star on the Hollywood Walk of Fame at 7048 Hollywood Boulevard. She also received TV Land Awards in 2004, 2006, and 2007 for her portrayal of Alice Nelson, the housekeeper on The Brady Bunch.
References
^ Jump up to: a b "Ann B. Davis Biography (1926–)". Film Reference. Advameg, Inc. Retrieved February 1, 2014.
^ Jump up to: a b c d e f Moran, Elizabeth (1992). Bradymania! Everything You Always Wanted to Know – and a Few Things You Probably Didn't. Adams Publishing. pp. 114–115. ISBN 1-55850-418-4.
^ Jump up to: a b "Ann B. Davis Biography". TV Guide. CBS Interactive Inc. Retrieved February 15, 2014.
Jump up ^ Gliatto, Tom; Eftimiades, Maria; Abrahams, Andrew; Baker, Kathryn; Johnston, Jerry (June 1, 1992). "Here's the Story...". People. 37 (21). Retrieved February 15, 2014.
Jump up ^ "Famous Alumni". Alumni Association of the University of Michigan. University of Michigan. Retrieved March 28, 2014.
Jump up ^ Jukebox Jury: Research Video, Inc.: Music Footing Licensing Agency and Vintage Television Footage Archive
^ Jump up to: a b "From Schultzy to Alice to God: Comic Ann B. Davis Finds a New Role". People. 8 (7). August 15, 1977. Retrieved February 15, 2014.
Jump up ^ "Ann B. Davis". Hollywood Walk of Fame. Hollywood Chamber of Commerce. Retrieved February 15, 2014.
Jump up ^ Leszczak, Bob (November 2, 2012). Single Season Sitcoms, 1948–1979: A Complete Guide. McFarland. p. 97. ISBN 978-0-7864-9305-0. Retrieved February 15, 2014.
Jump up ^ "Ann B. Davis Biography". The Biography Channel. A+E Television Networks, LLC. Retrieved February 15, 2014.
Jump up ^ Stoneback, Diane (May 3, 1995). "Hey, Alice! What's for dinner?". The Spokesman-Review. Retrieved February 15, 2014.
Jump up ^ Jacobs, Matthew (April 5, 2013). "The 'Brady Brunch' Cast: Where Are They Now?". The Huffington Post. Retrieved February 15, 2014.
Jump up ^ Droganes, Constance; Dagostino, Mark; Cascerceri, Dorothy; Pitluk, Adam; Lopez, Molly; Brunner, Jeryl (April 12, 2004). "Daily Insider for April 13, 2004". People. Retrieved February 15, 2014.
^ Jump up to: a b Dam, Julie K.L.; Miller, Samantha (December 13, 1999). "The Family Still Matters". People. 52 (23). Retrieved February 15, 2014.
Jump up ^ "TV's Ann B. Davis takes religious role". Chicago Sun-Times – via HighBeam Research (subscription required). July 15, 1991. Retrieved February 15, 2014.
Jump up ^ "Ann B. Davis". biography.com. Retrieved June 2, 2014.
Jump up ^ "Brady Bunch actress dies," Laredo Morning Times, June 2, 2014, p. 10A
Jump up ^ Shoichet, Catherine E. (June 1, 2014). "Ann B. Davis, Alice on 'Brady Bunch,' dies". CNN. Retrieved June 1, 2014.
Jump up ^ Barnes, Mike (June 1, 2014). "'Brady Bunch' Star Ann B. Davis Dead at 88". The Hollywood Reporter. Retrieved June 1, 2014.
Jump up ^ "The Brady Bunch: Ann B. Davis Dies at 88; Farewell Alice Nelson". tvseriesfinale.com. June 1, 2014.
Jump up ^ Peltier, David (2014). "Ann B. Davis". Find a Grave memorial 130713720 with biographical profile and related photographs created June 1, 2014. Retrieved May 9, 2017.
^ Jump up to: a b c "Brady Bunch housekeeper Ann B. Davis won two Emmys". The Sydney Morning Herald. June 2, 2014. Retrieved June 2, 2014.
^ Jump up to: a b c d e Chawkins, Steve; Parker, Steve (June 1, 2014). "Ann B. Davis dies at 88; actress best known for 'Brady Bunch' role". Los Angeles Times. Retrieved June 2, 2014.
Jump up ^ "Ann B. Davis: 12 Things You Didn't Know About the 'Brady Bunch' Star". Variety. June 1, 2014. Retrieved June 2, 2014.
Jump up ^ Stedman, Alex (June 1, 2014). "Ann B. Davis, Alice on 'Brady Bunch,' Dies at 88". Variety. Retrieved 4 June 2014.
Biography portal
New York portal
Pennsylvania portal
Greater Los Angeles portal
California portal
Texas portal
Television portal
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Theatre portal
Christianity portal
External links
Wikimedia Commons has media related to Ann B. Davis.
Ann B. Davis on IMDb
Ann B. Davis at the Internet Broadway Database
Ann B. Davis Archive of American Television Interview
Ann B. Davis at Find a Grave
[hide]
v
t
e
Primetime Emmy Award for Outstanding Supporting Actress in a Comedy Series
Vivian Vance (1953)
Audrey Meadows (1954)
Nanette Fabray (1955)
Pat Carroll (1956)
Ann B. Davis (1957)
Ann B. Davis (1959)
Alice Pearce (1966)
Frances Bavier (1967)
Marion Lorne (1968)
Karen Valentine (1970)
Valerie Harper (1971)
Sally Struthers / Valerie Harper (TIE) (1972)
Valerie Harper (1973)
Cloris Leachman (1974)
Betty White (1975)
Betty White (1976)
Mary Kay Place (1977)
Julie Kavner (1978)
Sally Struthers (1979)
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Eileen Brennan (1981)
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Carol Kane (1983)
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Julie Bowen (2012)
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Allison Janney (2015)
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WorldCat Identities
VIAF: 21707009
LCCN: no91016515
IATH: w6hv7b8g
Retrieved from "https://en.wikipedia.org/w/index.php?title=Ann_B._Davis&oldid=794568995"
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