CHERTS
AND SILICEOUS SEDIMENTS
8
areas of high organic productivity, and also occur in some lakes. Relatively pure siliceous oozes are known as radiolarian or diatoma- ceous oozes, depending on the dominant microfossil component. Less pure siliceous sediments are informally known as sarls (siliceous muds) and smarls (siliceous calcare- ous muds). Por cellanite is a hard siliceous sed- iment, in which the original biogenic silica (opal-A) has transformed to the more ordered opal CT, but not completely to quartz. Diatomites, radiolarites and spiculites are also partly lithified sediments still rich in opal CT.
Principal sedimentary characteristics
See photographs and figures in the relevant sections of Chapter3as well as at the end of this chapter.
CHERTSare generally very hard, dense rocks, which splinter with a conchoidal fracture when struck. They are subject to intense dia- genetic recrystallization and remobilization that typically partially or completely obscures primary depositional features. Of the two main types, bedded cherts retain more of their original characteristics, including lamina- tion, cross-lamination, grading, etc. Colour depends on impurities, and ranges from white/pale grey (pure), through browns and reds (traces of iron), greens (traces of iron from chlorite or smectite clays in volcaniclas- tics), to darker greys and black (clays and organic carbon).
Bedding
Bedded cherts are generally 1 – 10cm thick, but may be >30cm thick, with slightly irregu- lar to wavy margins, commonly appearing within mudrock, volcaniclastic or limestone successions. Nodular cherts occur as ovoid to irregular nodules, very variable in size (long diameter typically 1 – 30cm), commonly con - centrated along bedding planes, and in some places coalescing to form semi-continuous irregular layers.
Structures
Bedded cherts are typically massive (either primary or diagenetic) or finely laminated (seasonal or current influence); cross-lamina- tion, graded bedding and micro-scour struc- tures are indicative of turbiditic cherts. Slump folding and synsedimentary brecciation are also evident in some cases.
Primary structures are mostly absent or poorly preserved in nodular cherts. In some cases the nodules form preferentially around a burrow network (e.g. Thalassinoides bur- rows), so that their overall form shows the trace fossil structure.
Texture
Many bedded cherts are dominated by an equant mosaic of microquartz crystals, together with some chalcedonic quartz, that effectively obscure original grain size charac- teristics; some do reveal original sand–silt– clay sized particles, including grading.
In nodular cherts, the original grain size texture is usually destroyed as dispersed bio- genic silica dissolves and reprecipitates as opal-CT at nodule growth points. At a later stage this matures to quartz.
Composition
In bedded cherts of biogenic derivation the original components are mainly siliceous microfossils (radiolarians, diatoms and sponge spicules), plus siliciclastic and calcare- ous impurities and, in some cases, relatively high traces of organic carbon and phosphates. Radiolarians and sponges occur in Cambrian to Recent sediments, whereas diatoms first appeared in the Triassic, remaining rare until the Cretaceous. These siliceous components are generally recrystallized to quartz, although careful examination may reveal remnant sand-sized spheres, discs and spines.
Nodular cherts are dominated by pure microquartz, macroquartz and chalcedonic quartz formed both as replacement and pore filling cement within the carbonate (or other) host sediment.
occur within limestone hosts, and less com- monly in mudrocks. The silica was originally biogenic and more widely dispersed through the pelagic or hemipelagic sediments. Primary biogenic lacustrine cherts and sil- cretes within soil horizons occur more rarely.
CHERTS
AND SILICEOUS SEDIMENTS
8
Major types
Bedded chert
Nodular chert
Partly lithified siliceous sediments Unlithified siliceous sediment Hybrid siliceous sediments Subtypes Radiolarian chert, diatomaceous chert, spicule-rich chert, black chert, jasper
Flint Silcrete Radiolarite Diatomite Spiculite Porcellanite Siliceous ooze Sarl Smarl Siliceous limestone Siliceous tuff
Nature and origin
Mainly marine (some lacustrine) in origin; comprise part recrystallized quartz and part biogenic remains, plus minor impurities.
Nodular chert found in Chalk.
Nodular or encrusting chert formed in certain soils or as surface coating.
Rich in radiolarians. Rich in diatoms. Rich in sponge spicules.
Hard siliceous sediment (general term).
Soft unconsolidated siliceous sediment (general term).
Siliceous mud (unconsolidated).
Siliceous calcareous mud (unconsolidated). Siliceous carbonate sediment.
Siliceous volcaniclastic sediment. Table 8.1 Principal types of chert
FIELDTECHNIQUES
Cherts and other hard siliceous sediments have a distinctive ring when struck sharply with a hammer. They also show character- istic conchoidal fracture when broken. However, be very wary of sharp splinters that can fly off when struck, and are espe- cially dangerous to unprotected eyes.
Occurrence
CHERTSoccur in minor amounts throughout the geological record. In bedded cherts of Precambrian successions and in association with volcaniclastic sediments (especially those of acid or intermediate derivation), the silica may, at least in part, have a direct vol- canic origin. Other bedded cherts are most likely of primary biogenic origin, produced by the pelagic rain of siliceous planktonic organisms common below regions of high surface productivity. In some cases, shelf and upper slope siliceous sediments have been resedimented downslope yielding chert tur- bidites. Nodular cherts, on the other hand, are mostly of diagenetic origin. They typically
8.1 Core sections split lengthways showing parts of subrecent siliceous debrite unit, originally deposited as pelagic biogenic facies under the upwelling zone on Walvis Ridge. Sub-rounded and soft-sediment deformed clasts of organic-rich, siliceous facies (sarls, dark), and organic-poor, calcareous facies (marls–oozes, pale). Width of core 8cm. Plio–Pleistocene, Walvis Ridge, SE Atlantic Ocean.
8.2 Irregular, nodular band of dark flint within chalk. The bands are bedding parallel, and represent periods of time when there was an increased pelagic rain of siliceous tests to the sea floor. Dissolution, remobiliza- tion, and precipitation of the silica as irregular nodules occurred during burial dia - genesis. Width of view 35cm. Late Cretaceous, Isle of Wight, S England.
CHERTS
AND SILICEOUS SEDIMENTS
8.3 Detail of flint nodule within chalk. Note the white chalk (micrite) coating and dark grey interior of nodules.
See also caption for 8.2.
Width of view 20 cm. Late Cretaceous, Isle of Wight, S England.
8.4 Black organic-carbon-rich chert beds in limestone succes- sion. The chert beds represent periods of time with dominant accumulation of siliceous bio- genic material at the seafloor. Recrystallization during burial diagenesis has been largely in situ. The black colour in this case is due to preservation of organic carbon.
Width of view 6m.
Mid-Cretaceous, Umbro-Marche region, central Italy.
8.5 Thin chert bands/beds (pale) in dark sparitic limestone. Note dissolution seams between beds. Penknife 9cm.
Paleogene, central Crete.
CHERTS
AND SILICEOUS SEDIMENTS
8.6 Chert concretion (C) in dark sparitic limestone (as 8.5); note incipient formation of bedding-parallel stylolites (S) in limestone. Penknife 9cm. Paleogene, central Crete.
8.7 Large concretions of dark grey chert in limestone. Hammer 50cm. Photo by Paul Potter. Lower Carboniferous
(Mississippian), Gilbertsville, Trigg County, Kentucky, USA.
8.8 Calcilutite showing partial silicification in lenses (pale grey) and nodules (darker grey). Lens cap 6cm.
Jurassic, near Scaglia Bani, Sicily, Italy.
CHERTS
AND SILICEOUS SEDIMENTS
8 C
8.9 Organic-carbon-rich radiolarites and siliceous micrites; well-laminated upper section is mainly pelagic; more irregular beds are
debrite–turbidite (D,T) interca- lations.
Miocene, Monterey Formation, California, USA.
8.10 Thick-bedded radiolarite turbidite–debrite (arrow), with coarse clast-rich base and large floating clasts (F) and raft (R) about 1.5m up from base. Miocene, Monterey Formation, California, USA.
CHERTS
AND SILICEOUS SEDIMENTS
8
T
D D
8.11 Interbedded micrite and chert (darker layers, yellowish in parts). Many of the chert beds are of turbidite origin (lamina- tion and grading visible on close inspection), deposited within a mainly pelagic carbonate slope- basin setting. The yellowish colour derives from terrigenous impurities. Note cross-cutting faults with minor displacement. Width of view 1.2m. Paleogene, Lefkara, S Cyprus.
8.12 Chert beds (pale yellow- ish) in micrite; cherts are of turbidite origin deposited within a pelagic carbonate slope-basin setting. Beds steeply inclined; exposure covered with much loose rubble. See also caption for8.11. Width of view 3.5m. Paleogene, Lefkara, S Cyprus.
CHERTS
AND SILICEOUS SEDIMENTS
PHOSPHORITES
Favoured perch for cormorants leads to guano accumulation, central Chile. Photo by Claire Ashford. Chapter 9
192
Phosphorites are generally divided into three main groups (Table 9.1): bedded and nodular phosphorites, usually of marine origin and formed in association with high organic productivity; bioclastic lag phospho- rites (bone beds); and guano (bird or bat excrement) and its associated facies. Guano is not known from the ancient geological record and is not discussed further here.
Definition and range of types
SEDIMENTS and sedimentary rocks that are composed largely of phosphatic material are collectively known as phosphorites. Al though phosphorus is an essential component of all living matter, and the dominant constituent of vertebrate bones, phosphorites are relative- ly rare in the sedimentary record.
PHOSPHORITES
9 Principal sedimentary characteristics
See photographs and figures in the relevant sections of Chapter 3as well as at the end of this chapter.
PHOSPHORITES are relatively rare and not easily recognized in the field. They mostly occur as dark organic-rich sediment, slightly enriched in phosphate and as distinct phos- phatic nodules and crusts, with a dull black to yellow-brown coating. Bioclastic lag deposits are more restricted in occurrence. They are generally dark brownish-black, shiny, hard, and relatively resistant to weathering, but may become friable on breaking.
Bedding
The bedded/nodular phosphorites occur either as well-bedded layers, generally as thin beds; or as spherical, ovoid, tubular, and irregular nodules (typically 1–10cm diame- ter), commonly in distinct layers. Associated
facies include phosphatic mudrock, dolomite, and limestone. Bioclastic lag phosphorites are invariably well-bedded, and of variable thick- ness (generally <30cm).
Structure
Beds and nodules may display homogeneous or laminated structure, or a more chaotic con- glomeratic form. Lag deposits are typically more jumbled or chaotic, but with bed-paral- lel and current-parallel alignment of clasts evident in many cases.
Texture
Grain size varies from fine-grained mud- rock to sand-sized oolitic, pisolitic, and pellet - al texture. Concentrations of phosphatic nod - ules may appear conglomeratic. Lag deposits are generally very poorly sorted, of variable grain size, from fine mud matrix to elongate fecal pellets (up to 2cm), and larger phosphat- ic pebbles. Major types Bedded and nodular phosphorites Bioclastic lag phosphorites Guano Subtypes
Nodules and pavements, bioclastic phosphorites, pelletal and oolitic phos- phorites, phosphate-rich muds
Phosphatic bone beds
Phosphatic pebble beds
Bird guano Bat guano
Nature and origin
Formed in association with organic-carbon rich sediments under upwelling systems and enhanced organic productivity; open marine outer shelf/upper slope setting; range of facies depend- ing on local conditions and associated sediments.
Skeletal fragments (vertebrate bones, fish scales) and coprolites concentrated by currents/waves. Associated with slow deposition or hiatus. Reworked bone beds and (diagenetic) phosphate nodules.
Localized, thick accumulation of bird excrement. Localized, thick accumulation of bat excrement. (Both can be associated with phosphatization of underlying rocks.)
Composition
Most sedimentary phosphorites are carbon ate hydroxyl fluorapatites [Ca10(PO4,CO3) 6F2-3]; in some cases with a distinct miner - alogy (francolite, F-rich; dahllite, F-poor) but more often as the cryptocrystalline collophane. The P2O5content ranges from 5–35%.
In lag deposits, there are a wide variety of phosphatic clasts, phosphatized bioclastics and non-phosphatic material; faecal pellets and fish scales are also common.
Occurrence
MARINE PHOSPHORITESare well known from present-day and sub-recent occurrences along the outer shelf/upper slope regions of conti- nental margins that have enhanced organic productivity. They mostly form in low- oxygen rather than fully anoxic conditions, occurring as phosphatic pellets, nodules,
PHOSPHORITES
9
FIELDTECHNIQUES
Phosphorites are rare and not easily recognized in the field. If you suspect their occurrence, take samples back to the lab for thin-section and chemical analyses.
9.1 Phosphorite concretion (dark centre with white powdery surround) in mudrock. Lens cap 6cm. Paleogene, London Clay, S England.
Field photographs crusts, and thin beds; Evidence of current reworking is common. Ancient examples of this type are known from the Precambrian onwards, with apparent peaks in occurrence during the late Precambrian–Cambrian, the Permian, the late Cretaceous–early Tertiary, and the Miocene–Pliocene periods. These were periods of high sea level and widespread transgression leading to shallow, fertile shelf seas. Phosphorites are typical of condensed sequences, extremely low rates of sedimenta- tion, and the development of hardgrounds. Bioclastic lag deposits are more localized in occurrence, but significant as evidence of slow accumulation or hiatuses.
9.2 Phosphorite concretions (brownish-coloured) in dark- grey, organic-rich mudrock. Hammer 30cm.
Cretaceous, Speeton Clay, S England.
9.3 Detail of phosphorite concretions collected from various locations. Mostly brownish coloured, some with darker grey interior. Width of view 15cm. Jurassic, Oxford Clay, S England.
9.4 Phosphorite concretions around crab carapaces – the left one found in situ, the right one found reworked in glacial outwash deposit. Note the dull to shiny black colour typical of phosphatized remains. Width of view 10cm. Paleogene, London Clay, S England.
PHOSPHORITES
9.5 Detail of phosphorite nodule, in which the phospho- rite (francolite) is encasing and replacing limestone in glauconitic marl. The black- green grains are glauconite, which commonly co-occurs with phosphorite. Width of view 12cm Cretaceous, Isle of Wight, S England.
9.6 Limestone hardground, phosphatized and overlain by glauconitic marl. Knife 9cm. Cretaceous, Isle of Wight, S England.
9.7 Bedding-plane view of phosphatic horizon within a condensed limestone unit, known locally as the Ludlow Bone Bed; the numerous bio- clastic fragments are mainly phosphatized denticles and spines from a primitive agnathid vertebrate. Width of view 10cm. Silurian, Shropshire, England.
PHOSPHORITES
9.8 Phosphorite concretions (brownish-yellow colour) in glauconitic sandstone. Width of view 10cm. Age uncertain, Gambia.
9.9 Phosphorite and carbonate nodules in marlstone. Age uncertain, Gambia.
PHOSPHORITES
Outcrops of Middle Pennsylvanian coals, Eastern Kentucky. Photo by Jim Hower. Chapter 10
198
rocks. By definition they should contain <33% inorganic material (impurities) but generally they have <10% clay, silt, and sand, as well as a host of minerals present in minor and trace amounts. They are a very common (and economically important) sediment type that is easily recognized in the field.
Most coals are humic coals, formed from the in situ accumulation of plant material. Sapropelic (or drift) coals, by contrast, have formed from the dispersal and subsequent accumulation of broken-up plant debris, spores, pollen, and/or algae. Coal rank refers to the degree of metamorphism (or coalifica- tion) of the organic matter. Humic coals can be divided on the basis of their rank into a number of categories.
Definition and range of types
COAL AND OIL(including natural gas) are the two principal fossil fuels found in sedi - mentary rocks and, currently, the world’s dominant source of commercial energy. They have close parallels in their origin but signifi- cant differences in occurrence. Whereas coal is a common sedimentary rock, oil is a liquid fuel that is hosted or reservoired in sediments. They are also closely linked in that coal is an important source rock for gas and, in some cases, for oil too. Coal is the main focus of this chapter, but the origin and occurrence of oil is also described briefly.
Coals are brown to black, soft to hard, low-density, organic-carbon-rich sedimentary