Biostratigraphy of the Peri-Gondwana Cambrian trilobite fauna (northern Kerman, Iran) and

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Biostratigraphy of the Peri-Gondwana Cambriantrilobite fauna (northern Kerman, Iran) and correlationwith other countriesHamed Ameria & Fatane Zamaniba Department of Ecology, Institute of Science, High Technology and Environmental Sciences,Graduate University of Advanced Technology , Kerman, Iranb Department of Geology, Faculty of Sciences, University of Isfahan , Isfahan, IranPublished online: 29 Jun 2015.

To cite this article: Hamed Ameri & Fatane Zamani (2015): Biostratigraphy of the Peri-Gondwana Cambrian trilobite fauna(northern Kerman, Iran) and correlation with other countries, Historical Biology: An International Journal of Paleobiology,DOI: 10.1080/08912963.2014.927870

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Biostratigraphy of the Peri-Gondwana Cambrian trilobite fauna (northern Kerman, Iran) andcorrelation with other countries

Hamed Ameria* and Fatane Zamanib

aDepartment of Ecology, Institute of Science, High Technology and Environmental Sciences, Graduate University of AdvancedTechnology, Kerman, Iran; bDepartment of Geology, Faculty of Sciences, University of Isfahan, Isfahan, Iran

(Received 3 February 2014; accepted 21 May 2014)

Polymeroid trilobite fauna from two stratigraphic sections (Godbondar and Kuhbanan) of the Kuhbanan Formation innorthern Kerman (central Iran) were studied and subjected to biostratigraphic analysis. Eleven genera and species arerecognised from the latest Early Cambrian and Middle Cambrian Peri-Gondwanian successions of the study sections. Therecognised fauna includes Afghanocare lategenatum, Blountia blountia, Iranoleesia sp., Iranoleesia pisiformis, Kermanellakuhbananensis, Kermanella lata lata, Kermanella lata minuta, Kermanella sp., Redlichia chinensis, Redlichia noetlingi andRedlichia sp. Based on trilobite distribution, three trilobite biozones were recognised in the study sections, namely Redlichianoetlingi biozone, Kermanella kuhbananensis biozone and Iranoleesia pisiformis biozone. The age of the study sections islate Early Cambrian to late Middle Cambrian based on the recognised trilobite biozones. The recognised late EarlyCambrian trilobite assemblages (especially Redlichia and Kermanella) from northern Kerman are similar to those foundfrom some other parts of Gondwana or Peri-Gondwana terrains (north India, Pakistan, northwestern Kashmir, Tajikistan,South Australia, South China and Afghanistan) and show affinities with fauna found in some other parts of Iran (Alborz,northern Iran; Tabas, eastern Iran; southeast Karman).

Keywords: polymeroid trilobite; Cambrian; Kuhbanan Formation; Peri-Gondwana; central Iran

1. Introduction

Cambrian deposits are distributedwidely in different basins

of Iran. Each basin has distinct lithostratigraphic and

biostratigraphic characteristics and fossil contents. The

CambrianSystem in theAlborz andZagros basins (northern

and southeastern–northwestern Iran, respectively) consists

of upper parts of the Soltanieh Formation and Barut,

Zaigun, Lalun andMila Formations. The Cambrian System

in central Iran cropped out in two different sub-basins:

Kerman (southeastern Iran) and Tabas (eastern Iran). The

Cambrian deposits of northern Kerman sub-basin comprise

two series and three formations from base to top; they

include the Rizu and Dezu Series and Dahu, Kuhbanan and

Unnamed Formations. The above-mentioned deposits have

a thickness of 1000–2700m and consist of evaporite,

igneous and siliciclastic–carbonate rocks. (Almost all of

the deposits outcropped along the Kuhbanan fault.) The

Cambrian deposits of the Tabas sub-basin, Mila Group,

have a thickness of 1200–3100m and consist of evaporite

and siliciclastic–carbonate rocks. They are divided into the

Kalshaneh, Derenjal and Shirgesht Formations. Study on

the Cambrian trilobites of Iran started in the early twentieth

century. Iranian Cambrian trilobites have been studied by

many authors (King 1930, 1937; Wadia 1934; Balashova

1966; Wolfart 1974; Fortey and Rushton 1976; Kobayashi

1976; Kushan 1978; Wrona and Hamdi 2000; Ameri and

Dastanpour 2010; Ameri 2015). However, the biostrati-

graphy of the Iranian Cambrian trilobites remains poorly

documented.

Unfortunately, Iranian Cambrian trilobites are gen-

erally neglected in global assessments of Cambrian

stratigraphy and palaeontology. The Cambrian deposits

are widely distributed in Iran, but contain very few

fossils, such as the remains of brachiopods, gastropods,

stromatolites and trilobites (only in the Kuhbanan and

Mila Formations). Among these, trilobites are the most

abundant and diverse. Therefore, the study of Cambrian

trilobite fauna in the Cambrian successions is essential

for biostratigraphic and paleobiogeographic models in

Iran.

Based on the trilobite fauna, Iranian Cambrian

successions are deposited in two basins: the Alborz basin

(northern Iran) and central Iran (eastern and southeastern

Iran). Trilobite fauna in the Alborz basin include Lorasian

trilobites, whereas in the central basin (Kerman and Tabas

area) they include pre-Gondwana trilobites. Therefore,

these facies are comparable with Parahio-Spiti (northern

India) (Hayden 1904), Salt Range (Pakistan) (Kobayashi

1976), Hand Ward (northwest Kashmir) (Wadia 1934),

Rabut-Pamir (Tajikistan) (Balashova 1966), South Aus-

tralia (Paterson et al. 2007), South China (Kobayashi

1976) and Surkh Bum (Afghanistan) (Wolfart 1974).

This study aims to provide systematic descriptions of

the Cambrian trilobite taxa of Iran. It also attempts to

q 2015 Taylor & Francis

*Corresponding author. Email: [email protected]

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construct a biostratigraphic scheme for Series nos 1 and 2

of the Cambrian System in the Kerman sub-basin.

2. Regional stratigraphy

2.1. Godbondar section

Godbondar section (with coordinates 3084801700N,5684404000E) is located to the east of Bondar village (east

Zarand) (Figure 1). TheEasternZarandMountains, ofwhich

Godbondar is a part, are bounded by the Kuhbanan fault to

the west and the Bidou syncline to the east. In the Eastern

Zarand Mountains, the Precambrian and Lower Palaeozoic

successions cropped out, and can be divided frombase to top

into the Rizu and Dezu Series, and the Dahu, Kuhbanan,

Unnamed, Katkoyeh and Niur Formations.

This study is focused mainly on the Kuhbanan

Formation. However, it presents a brief description of all

of the pre-Devonian successions cropping out in the study

area. Rizu Series is composed of siliciclastic and igneous

rocks. Dezu Series is lithologically similar to Rizu Series,

but gypsum and dolomitic rocks are present in its upper

parts. The component rocks of both of Rizu and Dezu

Series show a chaotic pattern. Dezu Series consists of grey

and black dolomites with interbedded gypsum, sometimes

developed in sequences up to 40m thick. The Series also

contains black limestones, violet–red thin-bedded micac-

eous sandstones and siltstones. No fossils have been

reported from the Dezu Series (Zhang et al. 1991).

According to Ruttner et al. (1968), the Dezu Series is

comparable with the Soltanieh and Barut Formations of

northern Iran. If this point of view is correct, it implies that

the lower part of the Dezu Series is Late Precambrian in

age. The Dahu Formation is a red sequence that typically

consists of red sandstones and red sandy shales. Cross-

bedding and ripple marks are present in its sandstones.

There are interbedded fine-grained breccias, and also

coarse sandstones in the Dahu Formation; the latter often

contain well-rounded grains of cherts. In the Godbondar

section the Dahu Formation is up to 45m thick. The Dahu

Formation is coeval with the Lalun Formation (in Zagros

and Alborz). The light-coloured (sandstones and quart-

zites) top zone of the Dahu Formation can be correlated

with the top quartzite of the Lalun Formation. The

Kuhbanan Formation consists of 110–150m of fine-

grained, red–brown sandstones with dolomite lenses and

thick- to thin-bedded limestones. The lithological nature of

the Kuhbanan Formation is very variable; it can be divided

into three informal members, as follows:

. Member 1 consists of thick-bedded, white quartzite

with ripple marks, and chertic pebbles (up to 8 cm in

diameter).. Member 2 includes grey to dark, partly dolomitic,

thick- to thin-bedded limestone (80–120m) with

interbeds of marly limestone. The limestone beds, in

particular, bear numerous remains of trilobites,

brachiopods, gastropods and Orthotheca.. Member 3 consists of unfossiliferous brown-bedded

dolomite with dolomitic lenses.

According to the occurrence of Redlichia, the

Kuhbanan Formation is late Early Cambrian to Middle

Cambrian in age. The Kuhbanan Formation in this area is

disconformably overlain with Unnamed Formation car-

bonate deposits (Cam-Ordovician?) and disconformably

underlain by the ‘top quartzite’ of the Early Cambrian

Dahu Formation (Figure 2).

The Katkoyeh Formation comprises 80m of buff and

grey–green siltstones and silty calcareous mudstones and

limestones with an interbedded red siltstone horizon. The

Katkoyeh Formation is the counterpart of the Shirgesht

Formation of the Tabas sub-basin and upper part of the

Mila Formation (in Alborz). The Katkoyeh Formation in

the study area gradually changes into the Niur Formation

(Silurian clastic deposits). Likewise, the dolomite succes-

sions of the Unnamed Formation disconformably underlie

the Katkoyeh Formation.

In the study area, clastic rocks of theNiur Formation are

partly developed and comprise white quartzitic sandstones,

siltstones, green sandy limestones and pure limestones. The

limestones are fossiliferous and contain different fauna of

brachiopods, trilobites, corals and conodonts.

2.2. Kuhbanan section

Kuhbanan section (with coordinates 3183201700N,

5681700400E), the most fossiliferous and the most complete

section of the Middle Cambrian, with 205m thickness, is

located near Kuhbanan town (about 170 km northwest of

Kerman) (Figure 3). The lower boundary of the Kuhbanan

Formation with the Dahu Formation is distinguished by

sharp lithological changes, so that the red siliciclastic

rocks of the Dahu are covered by the basal white quartzite

of the Kuhbanan. This Formation is conformably covered

by the Bahram deposits, with a sharp faulted contact

(Figure 4).

The Kuhbanan Formation can be subdivided into four

informal lithological members, as follows:

. Member 1 consists of thick-bedded, white to light

grey quartzite with oblique bedding, ripple marks

and chertic pebbles. The quartzite passes laterally

into medium- to coarse-grained, red–brown

sandstone.. Member 2 includes a 75-m thick sequence of

whitish to grey–brown, sandy, weakly lithified

dolomite and/or sandstones. Regionally, the dolo-

mite is partly replaced by fine-grained, often friable,

massive and thin-bedded, red sandstones. The lower

part of the member contains unfossiliferous small

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chertic grains. Lateral changes are common in this

facies.. Member 3 is composed of grey to dark grey, partly

dolomitic or pseudo-oolitic, thick- to thin-bedded

limestonewith yellowish-brown to reddishweathering

interbeddedwith marly limestones. Themiddle part of

the limestones (from 30 to 65m) bears numerous

remains of trilobites, partly completed trilobites,

carapaces, brachiopods and gastropods. Orthotheca

are particularly numerous in coarse crystalline lime-

stone. The upper unfossiliferous part shows an

increasing content of dolomite and chertic layers.

. Member 4 includes the uppermost successions of the

uppermost Middle Cambrian Kuhbanan Formation.

This member with 35m thickness consists mainly of

fine-grained, red–brown, slightly solidified sandstone.

However, dolomitic lenses, grey to yellowish-brown,

bedded dolomite are present subordinately.

3. Material and methods

Rocks of theKuhbananFormationwere investigated and their

fossil contents sampled systematically at two stratigraphic

sections (Godbondar and Kuhbanan). All in situ and

Figure 1. (Colour online) Location of Godbondar section in northern Kerman, central Iran, with dark areas representing mountains inthe Kerman to Saghand region, and geological map of the study area.

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identifiable fossils were collected. In total, 300 specimens

were collected from the study sections. All materials were

deposited at the Institute of Science, High Technology and

Environmental Sciences, in Kerman, Iran (ISHE).

The examined materials were prepared from marly

limestones using a vibro tool. The specimens were coated

with ammonium chloride to heighten the contrast before

being photographed using ring-light illumination. In most

cases, additional highlight from the northwest quadrant

was used. Photographs were taken using a Nikon D90

digital camera with a 105-mm objective. Apart from

digital sharpening, deepening of contrast and blackening

of the background, the photographs have not generally

been retouched.

4. Biostratigraphy

Thebiostratigraphic zonationproposedhere for theCambrian

System of the Kerman sub-basin is based on the local

occurrence ofwell-known trilobite taxa. The term ‘zone’ was

appliedwhen the eponymous species occurred inmore than a

single bed. Intervals of ‘no zonation’ are indicated in thick,

apparently barren, strata between the recognised zones,

where further work is required to clarify the biostratigraphy.

Biostratigraphic study of Kuhbanan and Godbondar

sections enabled the authors to develop a biostratigraphic

scheme with three trilobite zones for the Cambrian System

of the study sections (Figures 2 and 4). Recognised

trilobite zones spanned from stage 4 to the middle of

Guzhangian Stage. In ascending order, they are the

Figure 2. Stratigraphic section and taxon range chart of the Kuhbanan Formation, Godbondar section.

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Redlichia noetlingi zone, the Kermanella kuhbananensis

zone and the Iranoleesia pisiformis zone. The main

characteristics of the recognised biozones are as follows.

4.1. Redlichia noetlingi zone

The base of this biozone is characterised by the first

appearance datum (FAD) of Redlichia noetlingi and the

upper part of biozone is consistent with the last appearance

datum (LAD) of Redlichia noetlingi. Redlichia noetlingi

ranges from the uppermost Lower Cambrian to the

lowermost Middle Cambrian (Wolfart 1974; Ameri and

Dastanpour 2010), which is comparable with Shihchiao-

Sanshih stages in China. According to the global

chronostratigraphic criteria, Redlichia noetlingi ranges

from the late Early Cambrian to the lowermost Middle

Cambrian, which is comparablewith the Cambrian Series 2

(stage 4). The first sample of Redlichia noetlingi occurs

72m from the base of Godbondar section and 120m from

the base of Kuhbanan section. This zone includes Redlichia

noetlingi, Redlichia chinensis and Redlichia sp. The

Redlichia noetlingi zone is characteristic of member no. 3

of both study sections. Redlichia noetlingi has been

reported from the late Early Cambrian in some sections

from Iran (Wolfart 1974; Ameri 2015), Afghanistan

(Wolfart 1974), China (Kobayashi 1976), South Australia

Figure 3. (Colour online) Location of the Kuhbanan section in northern Kerman, central Iran, with dark areas representing mountains inthe Kerman to Saghand region, and geological map of study area.

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(Paterson et al. 2007) and the Pakistan Salt Range

(Kobayashi 1976). This biozone includes up to 20m of the

study sections. Trilobite taxa were commonly collected

from several horizons (sometimes in different lithology).

4.2. Kermanella kuhbananensis zone

This zone begins with the FAD of Kermanella kuhbana-

nensis. The species of Kermanella kuhbananensis ranges

from the lowermost Middle Cambrian (Cambrian stage 5)

to the Early Drumian stage, which is comparable with

Tangshih (Chinese stage). The first samples of Kermanella

kuhbananensis and Kermanella lata lata occur 96m from

the base of the Godbondar section and 140m from the base

of the Kuhbanan section, which indicates the Cambrian

stages 4 and 5 boundary. This zone contains Kermanella

kuhbananensis, Kermanella lata lata, Kermanella lata

minuta, and Kermanella sp. The upper limit of the interval

is defined by the LAD of Kermanella kuhbananensis.

Kermanella kuhbananensis has been reported from the

Middle Cambrian in the same sections in Iran (Wolfart

1974; Ameri and Dastanpour 2010; Ameri 2015).

4.3. Iranoleesia pisiformis zone

The base of this biozone is characterised by the FAD of

Iranoleesia pisiformis and the upper part of the biozone is

consistent with the LAD of Iranoleesia pisiformis.

Iranoleesia pisiformis is indicative of the uppermost Middle

Cambrian (Wolfart 1974; Ameri and Dastanpour 2010),

Figure 4. Stratigraphic section and taxon range chart of the Kuhbanan Formation, Kuhbanan section.

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which is comparable with Kushanian stages in China.

According to the global chronostratigraphic criteria,

Iranoleesia pisiformis ranges from the Late Drumian stage

to the Early Guzhangian stage. The first sample of

Iranoleesia pisiformis occurs 180m from the base of the

Godbondar section and 190m from the base of theKuhbanan

section. This zone includes Blountia blountia, Afghanocera

lategenatum, Iranoleesia pisiformis and Iranoleesia sp.

5. Biogeographic considerations

The late Early Cambrian trilobite assemblages recognised in

central Iran show affinities with fauna found in some other

parts of Gondwana or Peri-Gondwana terrains (Figure 5)

The Redlichia noetlingi zone is found in six sections in

northern Kerman, namely Charmis, Dar Abe, Dahu,

Katkuh, Akbarabad and Banestan. Redlichia noetlingi,

which is characteristic of this assemblage, is known only

from central Iran.

Redlichia nobilis, which is recorded from South China

and the Pakistan Salt Range, is very similar to some of the

redlichiids of the central Iran that are assigned to Redlichia

noetlingi.

The Kermanella kuhbananensis zone is reported only

from Kerman region. It shows weak affinities with Pakistan

Salt Range andSouthChina by the occurrence ofAnomocare,

a Salt Range genus that is closely related to the Kermanian

genus Kermanella and the Chinese genus Shantungarpis.

The Iranoleesia pisiformis zone is found at several

localities: southern and northern Kerman (Wolfart 1974;

Ameri 2015), northern Iran (Mila Formation) (Kushan 1978),

Surkh Bum, Afghanistan (Wolfart 1974) and the Pakistan Salt

Range (Kobayashi 1976). It shows medium affinities with the

southern China platform and Australia by the occurrence of

Lioparia, a Chinese genus that is closely related to the

Australian genus Leiopyg olaevigala. This assemblage is

similar to some species of the eastern IranianLioparellagenus.

The biogeographic message of these assemblages seems

clear. The Antarctic faunas do not show any close similarity

with faunas from other geographic regions of the rest of

Gondwana. Thus, althoughGondwanawas a huge continent,

itmust have been located atmedian latitudes in the Early and

Middle Cambrian so that trilobite faunas could spread

widely across its marginal seas (Palmer and Rowell 1995).

The apparent faunal differences may be mainly due to

local habitat conditions. They could also be affected by the

availability of fossiliferous horizons in Peri-Gondwana

province. However, in the Cambrian, Gondwana must

have become isolated from Laurentia, another Cambrian

continent that occupied lower latitudes.

6. Systematic palaeontology

Some of the taxa that aremore abundant andmost important

for biozonation are described below. The measurements

used are illustrated in Figure 6.Measurements, terminology

and abbreviations are derived from Shaw (1957), Kaesler

et al. (1997), Sundberg and McCollum (1997, 2000, 2003)

and Ameri and Dastanpour (2010). Sagittal (sag.) and

exsagittal (exsag.) measurements refer to lengths, whereas

transverse (trans.) measurements refer to widths.

Class Trilobita (Walch, 1771)

Order REDLICHIIDA (Richter, 1932)

Suborder REDLICHIINA (Harrington, Henningsmoen,

Howell, Jaanusson and Lochman-Balk, 1959)

Superfamily REDLICHIACEA (Poulsen, 1927)

Family REDLICHIIDAE (Poulsen, 1927)

Genus Redlichia (Redlichia) (Cossmann, 1902)

Redlichia noetlingi (Redlich, 1899)

Type species Hoeferia noetlingi (Redlich, 1899)

(Figures 7(a),(b),(e) and 8(a),(b),(e))

1899. Hoeferia noetlingi ver. Late et angusta n. g. et n.

sp. – Redlich, Cambrian fauna Salt Range, p. 3–

4, Pl. 1, Fig. 1–8.

1910. Redlichia noetlingi (Redlich) – Reed, Cambrian

fossils Spite, p. 7–9, Pl. 1, Fig. 14.

1930. Redlichia chinensis Walcott – King, Cambrian

fauna Persia, p. 316–318, Pl. 17, Fig. 1.

1937. Redlichia chinensis Walcott. – King, Cambrian

trilobites Iran, p. 4–5, Pl. 1, Fig. 2(a)–(c).

1941. Redlichia noetlingi (Redlich) – King, Cambrian

fauna Salt Range, p. 3–10, Pl. 1, Fig. 1–3, Pl. 3,

Figs 1–9, Pl. 4, Fig. 1–6.

1955. Redlichia noetlingi (Redlich) Schindewolf and

Seilacher, Kambriun Salt Range p. 293–299,

Abb. 1–5, Pl. 6, Fig. 1–15, Pl. 7, Fig. 1–6.

1962. Redlichia cf. chinensis Walcott. Huckriede,

Kursten and Venzlaff, Geological Kerman, p.

35–39.

1962. Redlichia noetlingi (Redlich)/nobilisWalcott/Group-

Huckriede, Kursten and Venzlaff, Geological Ker-

man, p. 35.

1962. Redlichia chinensis Walcott and Redlichia nobilis

Walcott – Kobayashi, Cambrian Eastern Asia,

p. 492.

Materials: Four fragments were collected, mostly

cephala and genalspain.

Description: This species is a characteristic micro-

pygous, with a large cephalon, having opistoparian facial

sutures. The cranidium is large to medium size, length 37–

17mm, width high convexity (sag. and trans.). The

cranidium has a parallel-sided glabella, S1 (trans.)

glabellar furrow, eye ridges directed moderately poster-

olaterally, and moderately wide fixigena (71 ^ 8%

glabellar width). The cranidium area covers about 66–

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70% of the cephalon, and the anterior border furrow angle

is 120 ^ 58. Anterior width (J2) in relation to cranidial

width (J1) is 70 ^ 2%. Cranidial width (J1) in relation to

cranidial length (A1) is about 53–65%. The preglabellar

field is flattened with tropidium relief in the anterior border

of the preglabellar area. The occipital ring is in relief and

wide, and the occipital furrow is deep and protracted. The

eye ring starts from the anterior branch, with a trend of 308.The glabella is pear shaped and in relief. The preocular area

is absent. The palpebral area is small and limited. The

ocular lobe shows very sharp relief, with a narrow terocular

area. The glabella has three lobes: S1 is completed, S2 has

a deeper furrow and S3 has two branch-lines at the end.

Distribution: Redlichia biozone, Kuhbanan Formation

(north Kerman), Hormoz Formation (southwest Iran), Salt

Range (Pakistan), Himalayan region, southern Siberia,

Australia and south of China.

Redlichia noetlingi has been regarded as late Early

Cambrian in age.

Order PTYCHOPARIDA (Swinnerton, 1915)

Suborder PTYCHOPARIINA (Richter, 1933)

Superfamily ASAPHISCACEA (Raymond, 1924)

Family ASAPHISCIDAE (Raymond, 1924)

Genus Anomocarella (Walcott, 1905)

Kermanella kuhbananensis (Wolfart, 1974)

Type species Anomocarella chinensis

(Figures 9(h), 10(a)–(c), 11(b) and 12(d))

1930. Anomocare megalurus (Dames) – King,

Cambrian fauna Persia, p. 318, Pl. 17, Fig 4.

1962. Anomocare megalurus (Dames) – Huckriede

et al., Geology Kerman, p. 35.

1962. Alokistocariden? – Huckriede et al., Geology

Kerman, p. 38 (Chabdjereh), p. 40 (Charmis).

1967. Protolenoid (Anomocare megalurus) Kobayashi,

Cambrian Eastern Asia, p. 492.

Materials: In total, 102 samples were collected, mostly

cephalon and pygidium.

Description: The glabella has a cylindrical shape, with

basal convexity towards the thorax. The occipital ring is

convex and covers about 16–20% of the glabellar area.

The occipital furrow is deep and protracted; this species is

characterised by three lateral lobes, and S1–S3 have two

branch-lines with 508 trend at the end. The frontal lobes

Figure 5. Correlation of the Cambrian System between northern Kerman and other continents.

Figure 6. Measurement lobe and furrow labels used in thetrilobite descriptions.

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are proximity flattened and show a relief from theirs upper

said to the preglabellar field. S1 has the deepest and widest

furrow. The glabellar field occupies about 41–45% of the

total cranidium area. The preglabellar field is wide and

flattened, and occupies about 14–16% of the cranidium

area. The eye ridge is in relief and parallel to the margin of

the preglabellar field. The preglabellar furrow is deep and

V-shaped. The posterior area is wide and proximately

flattened. The cranidium is wide (J1) in relation to its

length (A1), 50–57%, and the length of the occipital ring

(C) in relation to cranidium length (A1) is 25–28%.

Kermanella kuhbananensis is attributed to the early

Middle Cambrian (Drumian stage) in age.

Occurrence: The taxa were found 96m from the base

of Godbondar section.

Sample numbers: 1252 ISHE and 1253 ISHE.

Order PTYCHOPARIIDA (Swinnerton, 1915)

Suborder PTYCHOPARIINA (Richter, 1932)

Superfamily ASAPHISCACEA (Matthew, 1887)

Family ASAPHISCACEA (Raymond, 1924)

Genus Kermanella lata minuta (Wolfart, 1974)

(Figures 5(e) and 12(c))

Diagnosis: A sub-type of Kermanella lata with a broad

cranidium (average length) at 63% of the base width, wide

interocular fixed cheeks (on average 85% glabellar width),

small eyes (big eye index, on average 21%) and very

slightly divergent branches in the front seam.

Description: The outer contour of the cephalon is wide

and U-shaped, with short legs, slightly separate, posterior

margin in the area of the neck ring to the back, sides almost

Figure 7. All figures are dorsal view: a, b, e, Redlichia noetlingi, cranidium, £ 3; d, Redlichia chinensis, cranidium, £ 3; c, Redlichiasp., cranidium, £ 2.

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straight, slightly angled to the rear running outside. The

front median border is slightly wider than the sides, and

much narrower (sag.) than the preglabellar field. The

frontal border furrow has a weak side, becoming shallower

backward. Behind border of the eyes is wider and larger

than their inside border. The neck ring represents a rather

broad (sag.) laughing-shape, with a narrow side at the

posterior margin. The neck furrow is shallow, transversely.

Back furrows are shallow, curved, very slightly convex,

slightly convergent forward and united from the front to

back furrow.

The glabellar outline has a dented rear edge and is

similar to that of Kermanella kuhbananensis, but its

anterior margin is slightly convex. The measured

cranidium length in 10 samples involves 57%–68% of

the cephalon. Preglabellar cranidial sections are less than

half of the neck rings lengths. The interocular fixed cheeks

are very wide; so that our investigations on the 10 samples

show that they involve 77–93% of the glabella. The

palpebral lobes are very small and slightly curved, with a

long eye. The eye strips are poorly developed, only slightly

curved inwards and extending obliquely forward, as the

front glabellar corners plunge back into the furrows. The

front seam branches diverge forward, curving slightly to

10 ^ 58, the seam extending rear branches are slightly

curved convexly forward, obliquely rearward outwardly,

and bend only in the region of behind it, but backwards.

Owing to the median position of the eyes and the course of

the seam behind the branches, the fixed cheek rear sections

are comparatively long (sag.) and wide (trans.). In side

view, the apex line is extended to the apex plane or it is

inclined very slightly to the front on the neck ring.

Figure 8. All figures are dorsal view: a, b, e, Redlichia noetlingi, cranidium, £ 3; c, Redlichia chinensis, cranidium, £ 3; g, Redlichiasp., cranidium, £ 2; f, Kermanella kuhbananensis, thoracic segments, £ 4.

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Gradually, the apex line then tends somewhat more

forward, until approximately from S3 to the entire front to

the leading edge the cranidial part slopes quite evenly. The

preglabellar field and front hemline rut are cause very

slight undulations over the crest line. The front view is

dominated by the relatively small total curvature of the

cephalon. The strongest cross bow is the neck ring, the

glabella rises only slightly above the general surface, fixed

interocular cheeks arch across very small free cheeks, and

the fixed cheek rear sections weakly slope outwards below.

The hypostome and pygidium are unknown.

Relations: Kermanella lata lata. The eyes are bigger

than minuta. The cephalon is positioned behind the centre.

It has a long eye index, on average 31% of minuta, a

deviating course of the back seam branches, and

differently shaped fixed cheek rear sections.

Time: Because of the association with Redlichia

noetlingi, it is only average to younger Lower Cambrian

in age.

Superfamily ASAPHISCACEA (Matthew, 1887)

Family ASAPHISCACEA (Raymond, 1924)

Genus Kermanella lata lata (Wolfart, 1974)

(Figures 9(d) and 11(c),(f))

1962. Alokistocariden, Huckriede, Kursten, Venzlaff,

& fur Bodenforschung, Geology Kerman, p. 37.

Description: The features mentioned below have not

been described for Kermanella kuhbananensis until now.

The outer contour of the cephalon is wide and U-

Figure 9. All figures are dorsal view: a, b, c, e, Afghanocare lategenatum, cranidium, £ 5; d, Kermanella lata lata, cranidium, £ 6; f,Blountia blountia, cranidium, £ 6; g, Kermanella sp., cranidium, £ 5; h, Kermanella kuhbananensis, cranidium, £ 6.

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shaped, with short, slightly curved backward inside legs,

the rear edge of the neck ring portion bulges rearward

laterally, slightly curved rearwards and outwards. The

front hemline median is slightly wider (sag.) than the

side, the front hemline rut weak side seam furrow is

only vaguely developed. It is difficult to say that the

neck ring nodules are developed in K. lata lata, because

of their unfavourable conservation. The neck furrow is

weakly pronounced, as are the back furrows, which are

curved slightly concave, and unite before the glabella

to the end union, the back furrow is shallow, and this

is about the same width as the back longitudinal

furrows.

The glabella in outline is like Kermanella kuhbana-

nensis, except that the leading edge is sometimes slightly

curved convexly.

The measured cranidium length in 10 samples involves

55% and 70% of the cephalon. The preglabellar cranidial

section is less than half as long as the glabella (with neck

ring), before the glabella is weaker than the convex side

(sag.). The intraocular hard-cheeks are arched transver-

sely; so that our investigations on the 10 samples show that

they involve 75–91% of the glabella. The palpebral lobes

are slightly curved, and the eye plate index is between 25%

and 38%, somewhat higher than in Kermanella kuhbana-

nensis. Eye strips on the inside of the clear cranidium are

formed in a convex arc, the front end to the front of the

connecting through the back palpebral lobe furrow through

the glabella (range between S3 and S4). The intraocular

transfixed cheeks are hardly curved, slightly inclined

outwards. The fixed cheeks rear sections are comparatively

long (trans.) and narrow.

Figure 10. All figures are dorsal view: a, b, c, Kermanella kuhbananensis, a, b, complete exoskeleton, £ 4, c, cranidium, £ 5; d,Kermanella sp., complete exoskeleton, £ 3; e, f, Redlichia sp., librigena, £ 3.

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The front seam diverges at an angle of about 10–158 tothe front hemline and turns closely bowing forwards

inside. Behind the seam, the first branches extend

obliquely rearwards and outwards, then turn at a fairly

large distance from the rear edge to the rear, and meet a

strong curve approximately at a right angle with the rear

edge.

In the side view, the apex line extends most pieces

from the neck ring to the rear edge S2, by the slightly

recessed neck furrow, broken below, almost at the apex

level, and sometimes even rising slightly. S2 is situated

before a gentle and gradual decline begins from the front

hemline rut. The flat to slightly domed front hemline fits

with a slight bend at the cranidium. Only a few pieces of

the end of the glabella are slightly more pronounced, so

that the apex line appears kinked. In front view, the entire

cephalon including the free cheeks as a very weakly

curved shield: the glabella is slightly convex, interocular

free cheeks are barely sprung, but the back grooves on the

outside are tilted weakly.

The pygidium in outline is transversely oval, and has a

curved outer edge which is slightly higher than the front

edge. Length of the pygidium is 1/3 of the cephalon length,

to the rear tapers only slightly, the rear border is blunt,

with a rounded front spindle ring curved sharply forward.

The furrow between the first and second rings is as wide as

the rings themselves. The second ring is hardly separated

from the rear undifferentiated stem section. Curved edges

are weakly curved with two or three low segments. Only

between the front two segments is a seam groove obtained.

A hem is thereby formed so that the grooves end in front of

the outer edge.

Figure 11. All figures are dorsal view: a, Kermanella sp., incomplete exoskeleton, £ 5; b, Kermanella kuhbananensis, completeexoskeleton, £ 4; c, f, Kermanella lata lata, complete exoskeleton, £ 4; d, e, Kermanella lata minuta, cranidium, £ 6; g, h, l, Iranoleesiapisiformis, cranidium, £ 4.

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Relations: Kermanella lata minuta. Distinguishing

features are known only from the head. Eyes small (sag.)

in median position, large eye index, average 21%. Fixed

cheeks rear sections rather long (sag.) and wide (trans.).

Time: Medium to younger Lower Cambrian, bearing

the Redlichia noetlingi (Sanshih Shihchiao-up stage?).

Family ORDOSIIDAE (Lu, 1954)

Subfamily CHELIDONOCEPHALINAE (Wittke, 1984)

Genus Iranoleesia (King, 1955)

Iranoleesia pisiformis (King, 1937)

(Figure 11(g),(h),(l))

1937. Irania pisiformis King, p. 12–13, Pl. 11, Fig. 6

(a)–(c).

1955. Iranoleesi apisiformis King, p. 86.

1967. Hundwarella pisiformis King Kobayashi, p. 493.

1976. Iranoleesia pisiformis King p. 330, Pl. 9, Fig. 6,

8–10 and 12.

1984. Iranoleesia pisiformis spinosa n., p. 106, Pl. 1,

Figs 12, 16 and 17.

Material: More than 40 cranidia, seven librigena, a

number of disarticulated fragments of thoracic segments,

and sex pygidium.

Occurrence: Kuhbanan Formation, Godbondar section

(ISHE 1997, ISHE 1996, ISHE 1992, ISHE 1993, ISHE

1994, ISHE 1998, ISHE 1980, ISHE 1981, ISHE 1972,

ISHE 1973, ISHE 1974, ISHE 1975, ISHE 1962 and ISHE

1952).

The glabella is forward tapering, with weakly curved

lateral margins. The front glabella is sub-truncate, with

Figure 12. All figures are dorsal view: a, d, Kermanella kuhbananensis, cranidium, £ 6; b, Kermanella lata lata, complete exoskeleton,£ 4; c, Kermanella lata minuta, cranidium, £ 4; e, Iranoleesia sp., cranidium, £ 5; f, Redlichia sp., librigena, £ 3; g, Kermanella sp.,cranidium, £ 5.

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shallow indention medially. The lateral glabellar furrows

are relatively faint on the exterior, but marked by an

absence of surface ornament; they are clearly visible

directly anterior to S3 in most specimens. The occipital

furrow consists of well-incised, slightly backward

directed lateral sections and a shallow median section.

Frontal indention of glabella created by fused parafrontal

sections at anterolateral corners, which extend over axial

furrows into the eye ridges. The eye ridges are nearly

straight, slightly backwards directed from the dorsal

furrows, moderately well defined on internal moulds,

faint on the external cuticle, clearly separated from the

palpebral lobes by narrow grooves. Palpebral lobes of

26–33% cephalic length, typically protolenoid, sausage-

shaped, convex in trans. section, straight in exsag.

direction. The preocular area has a moderately steep

ventral slope, anteriorly defined by a gently curved, deep

anterior border furrow. The anterior border furrow has a

clearly shallower and slightly posteriorly deviated median

section in front of the glabella created by a plectrum

developed as a slightly swollen, weakly defined ridge in

front of the glabella. The lateral borders of the plectrum

can be understood as shallow posteriorly curved sections

originating from the anterior border furrow to meet the

preglabellar furrow immediately in front of the anterior-

most projections of the anterior corners. Well-preserved

specimens show creases that cross the anterior border

furrow in front of the glabella. The cranidium area covers

about 50–61% of the cranidium, and the anterior border

furrow angle is 132 ^ 58. The anterior width (J2) relation

to cranidial width (J1) is 73 ^ 2%. The cranidium width

(J1) relation to cranidial length (A1) is about 73–75%.

The preglabellar field is flattened with tropidium relief in

the anterior border of the preglabellar area. The occipital

ring is in relief and wide, and the occipital furrow is deep

and protracted.

7. Conclusions

Trilobite fauna from two stratigraphic sections (Godbondar

and Kuhbanan) of the Kuhbanan Formation in northern

Kerman (central Iran) were studied and subjected to

biostratigraphic analysis.

Eleven genera and species are recognised from the

latest Early Cambrian and Middle Cambrian Peri-

Gondwana successions of the study sections. Recognised

fauna include Afghanocare lategenatum, Blountia bloun-

tia, Iranoleesia sp., Iranoleesia pisiformis, Kermanella

kuhbananensis, Kermanella lata lata, Kermanella lata

minuta, Kermanella sp., Redlichia chinensis, Redlichia

noetlingi and Redlichia sp.

The age of the study sections is late Early Cambrian to

late Middle Cambrian, based on recognised trilobite

biozones.

Based on the trilobite distribution, three trilobite

biozones were recognised in the study sections, namely

Redlichia noetlingi biozone, Kermanella kuhbananensis

biozone and Iranoleesia pisiformis biozone.

The late Early Cambrian trilobite assemblages (Red-

lichia and Kermanella) recognised from northern Kerman

are similar to those found from some other parts of

Gondwana or Peri-Gondwana terrains, Parahio-Spiti

(northern India) (Hayden 1904), Salt Range (Pakistan)

(Kobayashi 1976), Hand Ward (northwest Kashmir)

(Wadia 1934), Rabut-Pamir (Tajikistan) (Balashova

1966), South Australia (Paterson et al. 2007), South

China (Kobayashi 1976) and Surkh Bum (Afghanistan)

(Wolfart 1974), and show affinities with fauna found in the

Mila Formation (Alborz, northern Iran) (Kushan 1978),

Derenjal Formation (Tabas, eastern Iran) (Ruttner et al.

1968) and South East Karman (Ameri and Dastanpour

2010; Ameri 2015).

Acknowledgements

We extend warm thanks to Dr. Ebrahim Mohammadi for readinga draft version of the manuscript and making helpful suggestions.

Funding

This work was supported by the Institute of Science, HighTechnology and Environmental Sciences, Graduate University ofAdvanced Technology, Kerman, Iran [number 1.1869].

Disclosure statement

No potential conflict of interest was reported by the authors.

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