Microfacies Data: Matrix and Grains - Microfacies of Carbonate Rocks - page 154

Box 4.16. Selected case studies of ancient marine and non-marine (NM) ooids and ooid limestones.

Pleistocene: Caputo 1993; Evans and Ginsburg 1987; Fabricius and Klingele 1970; Geno and Chafetz 1982 (NM);
Hesse 1973; Jones and Goodbody 1984; Major et al. 1988; Richter and Neuser 1998; Wiedicke and Kudrass 1999
Tertiary: Roda 1965; Schoff 1937 (NM); Swirydczuk et al. 1979 (NM, low-salinity lake)
Cretaceous: Gely and Loreau 1986; Nazhat 1998; Simone 1974, 1981; Strasser 1986; Tisljar 1983.
Jurassic: Bausch 1961; Bersier 1937; Bosellini et al. 1981; Castellarin and Sartori 1973; Cussey and Friedman 1977;
d'Argenio et al. 1975; Dickinson 1969; Dragastan and Richter 1999; Fabricius 1967; Heydari and Moore 1994; Koch
et al. 1994; Kolckmann 1992; Loreau 1969, 1979; Martinis and Fontana 1968; Massari and Dieni 1983; Schaller and
Koch 1996; Schloz 1972; Scudeler Bacelle 1976, 1980, 1983; Sellwood et al. 1989; Strohmenger et al. 1987; Swirydcuk
1988; Wilson 1968; Zempolich and Erba 1999.
Triassic: Aigner 1984; Carozzi 1964 (NM); Fabricius 1967; Frantzen 1887; Friedel 1995; Gidon 1952; Haage 1970;
Hornung 1998; Kalkowsky 1908; Labecki and Radwanski 1967; Milroy and Wright 2000 (nonmarine, freshwater
lake); Paul 1982; 1985; Paul and Peryt 2000; Usdowski 1962, 1963; Young and Edmundson 1954; Zeng Yun-Fu
1983.
Permian: Bausch and Wiontzek 1961; Clark 1980; Füchtbauer 1968; Herrmann 1956; Kerkmann 1966; Piatkowski
1977.
Carboniferous: Burchette et al. 1990; Carozzi 1961; Choquette and Steinen 1985; Conley 1977; Dingle et al. 1993;
Feldman et al. 1993; Henbest 1945; Hird and Tucker 1988; Hunter 1993; Keith and Zuppann 1993; Kettenbrinck and
Manger 1971; Knewtson and Hubert 1967; Lacey and Carozzi 1967; Payton 1966; Wilkinson et al. 1984.
Devonian: Poncet 1983; Reijers and Ten Haave 1983.
Silurian: Richter 1983.
Ordovician: Cantrell and Walker 1985; Carozzi and Textoris 1965; Davis 1966; Hyeong and Lee 1992; Schramm 1963;
Stureson et al. 1999; Weaver 1992
Cambrian: Brown 1959; Carozzi 1963; Choquette 1955; Chow and James 1987; James and Klappa 1983; Mazzullo
1977; Poncet 1984; Sha and Jiang 1998; Swett 1965; Wherry 1916.
Precambrian: Beukes 1983; Labecki and Radwanski 1967; Radwanski and Birkenmayer 1977; Simonson and Jarvis
1993; Singh 1987; Sumner and Grotzinger 1993; Swett and Knoll 1989; Tucker 1984, 1985; Zempolich et al. 1988.

abundant in two periods: from the Ordovician to the
Devonian, and the Jurassic to the Early Tertiary (Young
1992).
Iron oolites were formed in more than one mode.
Microfacies studies of Devonian shallow-marine car-
bonates with iron ooids suggest that iron ooids origi-
nated in lagoonal or back-bar environments with tem-
porarily phreatic conditions and fluctuating Eh-pH con-
ditions. The iron was leached from pelitic sediments of
the Old Red continent and was precipitated as concre-
tionary iron hydroxide on bioclasts (Utescher 1992).
The Middle and earliest Late Jurassic oolitic ironstones
in central Europe originated in open, shallow to deeper
marine environments (Gygi 1981). Iron was derived
from the land by lateritic weathering. Iron ooids formed
at the distal fringe of an argillaceous, terrigenous sedi-
ment below the normal wave base but within the reach
of storm-generated waves.

Zempolich et al. 1988) exhibit distinct differences in
size, shape and internal structures. This has been ex-
plained by fluctuation in the concentration of calcium
carbonate in seawater during the Proterozoic (Grotzinger
1990). Estimate making according to the number of ref-
erences (Box 4.16), oolitic carbonates were abundant
in the Early Carboniferous and in the Middle and Late
Jurassic, but seem to have been rare in Silurian and Ter-
tiary deposits.

Secular variations
There is much evidence for temporal fluctuations in
the mineralogy of marine carbonate precipitates during
the Phanerozoic (Sect. 16.7.3). Sandberg (1983) postu-
lated a secular variation in the mineralogical composi-
tion of ooids with aragonite (and High-Mg calcite) oc-
curring in the Late Precambrian-Cambrian, Mid-Car-
boniferous through Triassic, and Tertiary to Recent, and
Low-Mg calcite ooids in the Mid-Paleozoic and Juras-
sic-Cretaceous. The temporal variation was explained
as a consequence of changes in the composition of ocean
water and the major controls on the mineralogy (P CO 2
and Mg/Ca ratio). Several authors prefer this model by
Bates and Brand (1990). Many exceptions to the gen-
eral pattern exist.

Ancient calcareous ooids: Ooids are known as far
back as the early Precambrian (Beukes 1983; Simonson
and Jarvis 1993: 2.5 billion years; ooids with radial-
concentric structures). Ooids from the Early and the
Late Precambrian (Radwanski and Birkenmajer 1977 ;
Singh 1987 ; Swett and Knoll 1989 ; Tucker 1984, 1985 ;