Trischizolagus of Tepe Alagöz

A new early Pliocene locality Tepe Alagöz (Turkey) reveals a distinctive tooth phenotype of Trischizolagus (Lagomorpha, Leporidae) in Asia Minor

Stanislav Čermák, Peter Joniak, and Bora Rojay

Article number: 22.1.14
https://doi.org/10.26879/924
Copyright Society for Vertebrate Paleontology, March 2019

Author biographies
Plain-language and multi-lingual abstracts
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Submission: 4 March 2018. Acceptance: 2 March 2019

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ABSTRACT

Pliocene leporid remains are very rare in Anatolia, occurring sporadically only in a few localities. The new locality of Tepe Alagöz (Çankırı Basin) is the first reported Pliocene locality in Turkey with sufficiently rich leporid material for determination of morphometric variability in taxonomically important teeth. The locality also yielded remains of the rodents Occitanomys debruijni, Allocricetus cf. ehiki, Pseudomeriones hansi, and an ochotonid lagomorph. The assemblage suggests an early Pliocene age (MN14) of about the same age or somewhat older than that in İğdeli (Sivas Basin). The medium-sized leporid is characterized by p3 of almost exclusively a “Nekrolagus” pattern with narrow anteroconid and very variable anteroflexid. It is associated with P2 bearing short paraflexus, long hypoflexus, and moderately developed mesoflexus, and I1 which is anteroposteriorly shortened with a shallow, V-shaped, cement-free anterior notch. The leporid was co-identified with Trischizolagus gambariani described from the coeval locality Nurnus (Armenia). A lectotype designation and emended diagnosis of the species are provided in this paper. The available fossil record of Trischizolagus indicates that the northwestern part of the peri-Paratethyan area was inhabited by T. dumitrescuae, but to the south and southeast by distinct T. gambariani. The only other proven finding of Trischizolagus from Anatolia was reported from Tozaklar (MN15), but due to the scarcity of fossil material a definite species determination is impossible.

Stanislav Čermák. The Czech Academy of Sciences, Institute of Geology, Rozvojová 269, 165 00 Prague 6, Czech Republic. cermaks@gli.cas.cz
Peter Joniak. Comenius University, Department of Geology and Paleontology, Mlynská dolina G, Ilkovičova 6, 842 15 Bratislava, Slovakia. peter.joniak@uniba.sk
Bora Rojay. Middle East Technical University, Department of Geological Engineering, 06531 Ankara, Turkey. brojay@metu.edu.tr

Keywords: Tepe Alagöz; Turkey; Pliocene; Rodentia; Lagomorpha; Trischizolagus gambariani

Čermák, Stanislav, Joniak, Peter, and Rojay, Bora. 2019. A new early Pliocene locality Tepe Alagöz (Turkey) reveals a distinctive tooth phenotype of Trischizolagus (Lagomorpha, Leporidae) in Asia Minor. Palaeontologia Electronica 22.1.14A 1-21. https://doi.org/10.26879/924
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Copyright: March 2019 Society of Vertebrate Paleontology.
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INTRODUCTION

Despite the fact that Pliocene terrestrial deposits occupy large areas in Turkey and fossil mammals of that age are reported from many localities—comprising MN14: Akçaköy, Aşaği Page, Babadat, Ҫeştepe, Elbistan, Hacisam, İğdeli, Kizilpinar, Yerlikuyu; MN15: Çalta, Ericek, Mahmutlar, Ortalica, Sürsürü, Taşova, Tekman, Tozaklar, Zirnak; MN16: Gülyazi, Kadiözü, Yenice (Ünay and de Bruijn, 1998; Şen et al., 1998, 2017, 2019; Ünay et al., 2003; Suata-Alpaslan, 2009a, 2009b, 2009c, 2010, 2012; De Bruijn et al., 2013; van den Hoek Ostende et al., 2015)—there are, in the vast majority of cases, scarce and fragmentary rodent associations. Moreover, compositions of available faunal assemblages are somewhat different from those of the surrounding regions (Şen et al., 2017). Thus, unsurprisingly, the Pliocene mammal faunas of Turkey are still poorly understood.

Fossil lagomorphs have been recorded in Anatolia in more than 60 localities aged between the early Miocene and middle Pleistocene (Şen et al., 2017, 2019). However, in contrast to the relatively well-recorded representatives of the family Ochotonidae, documented with six genera in about 50 localities, the record of Leporidae is very poor in only about 10 localities (Şen et al., 2017, 2019). The Pliocene leporids are limited only to Trischizolagus reported by Ünay and de Bruijn (1998) from Tozaklar (MN15) and Pliopentalagus reported by Suata-Alpaslan (2010, 2012) from Babadat (MN14), Akçaköy (MN14), and Tekman (MN15). The latter genus is referred to only in faunal lists without any descriptions.

The discovery of a new Pliocene locality in Turkey with a rich leporid record gives the opportunity to increase the knowledge and understanding of Pliocene leporid history in Asia Minor. In this framework, the aim of this paper is to: 1) describe the geological setting of Tepe Alagöz and its adjacent area (Çankırı Basin), 2) provide a stratigraphic correlation of fossil mammalian assemblage from Tepe Alagöz, 3) provide a detailed morphometric analysis of the leporid material under study, 4) redescribe and emend the diagnosis of Trischizolagus gambariani (Melik-Adamyan, 1986), and 5) hypothesize a possible evolutionary and dispersal history of the early leporids in Asia Minor.

GEOLOGICAL SETTING

Tepe Alagöz is located in the SE part of the Çankırı Basin (Figure 1), one of the key Neogene basins in Central Anatolia to the south of Pontides. The basin is situated on the ophiolitic mélanges and nappes of the Izmir-Ankara-Erzincan suture belt and bounded by the North Anatolian Fault Zone from north and Kırşehir Crystalline Complex from south.

The tectono-sedimentary evolution of the Çankırı Basin had mainly been controlled by the progressive closure of the northern Neotethys Ocean from the Late Cretaceous until the end of Miocene. During the Late Cretaceous-Paleogene, accretionary prisms and fore-arc basins were developed and followed by the Eocene age piggy-back to peripheral basins (Şengör and Yılmaz, 1981; Görür et al., 1998). Following the closure of the northern Neotethys during the Miocene, the region was characterized by an evolution of intracontinental, closed, and restricted fluvial-lacustrine basins on top of Oligocene sequences and Cretaceous ophiolitic imbricated nappes (e.g., Çankırı Basin; MN1-2 to MN14-15; Çiner et al., 2012; Mazzini et al., 2013; Şen et al., 2019) accompanied with extensive Neogene volcanism (e.g., Galatian volcanic province; 22 to 10 Ma) in northern Central Anatolia. After the collision of Eurasian plate with southern continental fragments - African and Arabian plates - during post-middle Eocene to late Miocene, the marine deposition in the Pontides ceased and retreated towards north (Paratethys), and to the southeast towards SE Anatolia to Basra (Iraq) (Şengör and Yılmaz, 1981).

The Çankırı Basin is developed on folded and southward-thrusted thick pre-Miocene sequences. The Oligocene gypsum-clastic sequence is overlain unconformably by early Miocene to early Pliocene sequences (Kaymakçı 2000) (Figure 2).

The Miocene Çankırı Basin can be differentiated into two parts: the western (Kalecik-Hancılı area) and the main central (Çankırı area). The early Miocene lacustrine basins on the western margin of the Çankırı Basin, under the effect of northward converging Kırşehir Block (Kaymakçı, 2000), continue as the middle to late Miocene fluvial to shallow lacustrine deposits in the rest of the Çankırı Basin (Lüttig and Steffens, 1976). During the latest Miocene-Pliocene, the Anatolian Plateau was fully covered by fluvial red clastics.

Deposition to the west was in two cycles: 1) the first was fluvio-lacustrine with swampy conditions where the mudrocks with limnic beds - even coal beds - developed in the earliest Miocene and 2) the second one was fluvio-lacustrine where red clastics and green-to-beige mudrocks with limnic beds developed during the early Miocene (Çiner et al., 2012) (Figure 2). The early Miocene mudrocks dominant along the western margin of the Çankırı Basin are missing in the rest of the basin. The early Miocene series in western Çankırı Basin are intensively folded and deformed compared to the uppermost early-middle Miocene ones in the rest of the basin. There is a possible tectonic saddle (elevated Cretaceous ophiolitic units) where an almost N-S sinistral strike-slip fault follows the saddle between the western parts and rest of the basin.

In the central part of the basin, the infilling sediments were deposited in two different sedimentary cycles during the Miocene: 1) the first were fluvio-lacustrine red clastics to green-to-beige mudrocks of the Burdigalian-early Serravalian (MN4-6?) fluvial red clastic deposition, in some places followed unconformably or gradually by Tortonian (MN9-11) mudrock-clastic sequences with limnic layers (Mazzini et al., 2013) and 2) the second one is made up of continental red clastics alternating upward with evaporites of middle to late Miocene age and the red beds of early Pliocene (Figure 2). The target lithology is a relatively undeformed sequence of sandstone to siltstone at Tepe Alagöz section, which are overlain by gypsum beds in the center of Çankırı Basin (Figure 1, Figure 2). Sampling was done along the southern limb of a broad syncline.

Briefly, the Miocene evolved completely within a fluvial to lacustrine depositional setting during the early Miocene (MN1-2) to early Pliocene (MN14) in an extensional basin. This basin evolved on top of an imbricated accretionary ophiolitic belt with a short gap during the late Serravalian (MN7-8 period). The steeply dipping to overturned Miocene deposits are overlain unconformably by the late Pliocene (MN17) fluvial red beds along the basin margins.

In summary, within the Miocene cycle, seven different depositional periods have been distinguished linked to progressive and intermittent indentation of the Kırşehir Block. These are (Figure 2): MN1-2 (Kılçak Formation) and MN2-3 (Altıntaş/Kumartaş Formation) in western margin of the Çankırı Basin; MN3-5 (Hançılı Formation); MN4-?6 (Çandır Formation); MN 9-11 (Tuğlu Formation); MN13-?14 (Süleymanlı Formation); and MN14-?15 (Bozkır Formation) in the rest of the basin.

MATERIAL AND METHODS

The described material was recovered from ~250 kg of sandy silt excavated in the locality Tepe Alagöz during summer of 2008. The sediment was processed following a conventional screen-washing procedure using a set of stable sieves with the small mesh size of 0.5 mm. The fossil remains were picked manually in the laboratory of Comenius University. The described material is stored in the Natural History Museum of the EGE University in Izmir (Turkey). The full format of specimen numbers is EUNMH PV30500, but in the following text we only use the format PV30500. Casts of the rodent teeth are stored in the collections of Department of Geology and Paleontology, Comenius University in Bratislava (Slovakia). Measurements were made using a calibrated micrometer eyepiece on the Leica MZ75 stereomicroscope. All dimensions are given in millimeters [mm]. Rodent teeth were photographed using an analytical SEM microscope Hitachi VP-SEM S-3700N, and lagomorph teeth were drawn using a camera lucida mounted on the stereomicroscope. Terminology used for teeth parts follows van de Weerd (1976) for Murinae; Daams and Freudenthal (1988), Cuenca-Bescós (2003) for Cricetinae; Tong (1989) for Gerbillinae; Şen (1998) for Ochotoninae; and Palacios and López Martínez (1980) and Čermák et al. (2015) for Leporinae. Morphotype classification used to describe teeth P2/p3 in Leporidae follows Fladerer (1987), Fladerer and Reiner (1996), Čermák (2009), and Čermák et al. (2015). The interspecific comparisons were made with the material held in the Department of Geology and Paleontology, Comenius University in Bratislava, Czech National Museum in Prague, Institute of Geology of the Czech Academy of Sciences in Prague, and/or on a bibliographical basis. Unless otherwise stated, data were taken from the original descriptions of species. Biostratigraphic terminology follows de Bruijn et al. (2013). All nomenclatural acts presented here conform to the mandatory provisions of the International Code of Zoological Nomenclature (ICZN, 1999).

Abbreviations. A0-A1 = general enamel p3 patterns of Leporidae defined by the combination of presence/absence of anteroflexid (sensu Čermák et al., 2015); BMR = buccal mesial reentrant (mesoflexus) of P2 in Leporidae; c1 = accessory posterior cuspid in m1 of Muridae; I/i = upper/lower incisors; L = length; LL = lingual lobe of P2 in Leporidae; M/m = upper/lower molars; MBR = major buccal re-entrant angle (hypoflexid) of p3 in Leporidae; max = maximum; min = minimum; N = number of specimens; OR = observed range; P/p = upper/lower premolars; Pa0 - Pa3, PR0 - PR4 = general enamel p3 patterns of Leporidae defined by the degree of development of paraflexid [Pa], and morphostructures between the trigonid and talonid [PR] (sensu Čermák et al., 2015); t1 - t12, t1 bis,and t2 bis = upper molar cusps of Murinae (sensu van de Weerd,1976); W = width; x̄ = arithmetic mean.

SYSTEMATIC PALEONTOLOGY

Class Mammalia Linnaeus, 1758
Order Rodentia Bowdich, 1821
Family Muridae Illiger, 1811
Subfamily Murinae Illiger, 1811
Genus Occitanomys Michaux, 1969
Occitanomys debruijni (Şen et al.,1989)
Figure 3.1-3

Material and measurements. 1 M1 dex, PV30500 (LxW = 1.90x1.42); 1 M2 dex, PV30501 (LxW = 1.42x1.24); 2 m1 dex, PV30502 (LxW = 1.75x1.14), PV30503 (LxW = -x1.02).

Description

M1. (Figure 3.1) The tooth has oval occlusal outline. The t1 is connected to the t5, while low connection to the t2 is through well-developed t1 bis. The t2 bis is weak. The t3 connects to the base of the t5 by posterior spur. There is a continuous circle connection between t4-t5-t6-t9-t12t-t8. The t7 is absent, and t12 is developed as a posteriorly placed, rounded cusp between the t8 and t9. The tooth has three roots.

M2. (Figure 3.2) The t1 is large and connected to the t5 and to the t1 bis. The t3 is small and tear-shaped. The high, circular connection between t4-t5-t6-t9-t8 is well developed. The t4 is connected to the base of the t8, and the t12 is absent. The tooth has three roots; two labial and one lingual that is wide and formed by intergrowth of two roots.

m1. (Figure 3.3) One of the two specimens is damaged in its anterior part. In the complete one the anterocentral cusp is absent, and the anteroconid cusps are connected to the protoconid-metaconid. The longitudinal spur is present in one specimen, while absent in the second one. The oval posterior tuberculum is well developed in both specimens. The c1 is developed as an elongated cusp connected to the base of hypoconid. Accessory labial cusp is on cingulum or as separate cusp. Both teeth have two roots.

Comparison and remarks. The teeth of Occitanomys debruijni from Tepe Alagöz are comparable in their size with those of the type material from Maritsa. They also fit in the upper size range of the type material of O. vandami described by Suata-Alpaslan (2009b) from İğdeli, but the M1 under study is slightly wider. However, de Bruijn et al. (2013, figure 26.2) mentioned from İğdeli only one species, O. debruijni. The differences between O. vandami and O. debruijni are subtle and we agree that O. vandami probably represents a synonym of O. debruijni. The material available from Tepe Alagöz is too scanty for statistical evaluation of morphological characters, but it shares discriminative features of O. debruini from its type locality of Maritsa (de Bruijn et al., 1970) and Develi (Şen et al., 1989). The material under study is also similar to that of O. debruijni from Tomea Eksi 2 (Hordijk and de Bruijn, 2009), but differs in having more developed posterior spur on t3, as in the type material from Maritsa (de Bruijn et al., 1970; Hordijk and de Bruijn, 2009). In contrast, M2 from Tepe Alagöz has only three roots while those from Tomea Eksi have four. Hordijk and de Bruijn (2009) stated that none of the M2 available from the type locality shows even an incipiently split lingual root, and this character is probably variable within the Occitanomys group.

Subfamily Cricetinae Fischer, 1817
Genus Allocricetus Schaub, 1930
Allocricetus cf. ehiki Schaub, 1930
Figure 3.4-5

Material. 1 M1 sin, PV30504 (LxW = 2.12x1.48); 1 M3 sin, PV30505 (LxW = 1.56x1.34).

Description

M1. (Figure 3.4) The anterocone is wide and splits into two equal cusps separated by the narrow central valley. The forked anterolophule connects to both anterocone cusps. The lingual branch of the anterolophule is stronger than the labial one. The protoloph is double; the posterior protolophule is better developed than the anterior one. The lingual sinuses are slightly deeper than labial ones. The parastyle is weaker than the mesostyle. The medium-long mesoloph connects to the metacone. The strong posteroloph is long, forming a posterolabial border of the tooth and connects to the metacone. Only the anterior root is preserved but the traces of three other roots are visible.

M3. (Figure 3.5) The labial anteroloph is strong and long, enclosing anterosinus, while lingual anteroloph is strongly reduced. The double protoloph forms a funnel between the protocone and paracone. The mesoloph is absent. The reduced metacone is fused in the ridge that encloses the posterior funnel. The tooth has three roots.

Comparison and remarks. The very limited material shows the morphological features typical for Allocricetus such as the 1) wide anterocone that is deeply split from behind, 2) double protolophule, and 3) absence of the metalophule and well-formed funnels between the main cusps. The overall morphology, size, and the presence of the parastyle and mesostyle support an attribution of the available material in A. ehiki. However, the material is very scanty, and since we do not have any lower molar, the above teeth are tentatively assigned here as Allocricetus cf. ehiki Schaub, 1930.

Subfamily Gerbillinae Gray, 1825
Genus Pseudomeriones Schaub, 1934
Pseudomeriones hansi Suata-Alpaslan, 2009a
Figure 3.6-8

Material. 1 M1 sin, PV30506 (LxW = 2.57x1.58); 1 M2 sin, PV30507 (LxW = 1.38x1.48); 1 m2 dex, PV30508 (LxW = 1.58x1.51).

Description

M1. (Figure 3.6) The tooth crown is high and its occlusal surface is rather narrow. The anterocone is placed slightly labially while the main cusps are clearly alternating. The anteroloph is in a line with the neoloph. The protosinus and sinus are equally developed and deeper than the mesosinus. The posterior sinus (sulcus) is small but clearly separates the posteroloph from hypocone. The roots are not preserved.

M2. (Figure 3.7) The occlusal surface is slightly concave. The protocone is more massive than other cusps. The anteroloph is small but distinctive while the posteroloph is developed as a wide oblique structure. The mesosinus is wide while the sinus is narrower and strongly curved backward. Both sinus and mesosinus are equally deep. Two roots are preserved; the anterior one shows a tendency for bifurcation.

m2. (Figure 3.8) The tooth has two main lobes separated by anteriorly directed sinusid and mesosinusid. The mesosinusid is longer and slightly deeper than sinusid. A shallow protosinusid is developed on the labial side of anterior lobe. A weak posterosinusid is outlined on the posterolingual side of the posterior lobe. The tooth has two roots.

Comparison and remarks. The tooth morphology of Pseudomeriones from Tepe Alagöz is almost identical to this of P. hansi from İğdeli described by Suata-Alpaslan (2009a). Slight differences, such as the 1) more pronounced posterior sinus (sulcus) in M1, 2) more developed anteroloph, and 3) unsplit anterior root in M2, seem to be ontogenetic because young and unworn specimens are predominantly represented in the assemblage under study. Sizes of available teeth from Tepe Alagöz are within the upper size range or slightly larger than those of P. hansi. Comparably large teeth of P. latidens and P. tchaltaensis differ morphologically.

Order Lagomorpha Brandt, 1855
Family Ochotonidae Thomas, 1897
Subfamily Ochotoninae Thomas, 1897
Ochotona seu Ochotonoma sp.
Figure 4.1-2'

Material and measurements. P2 sin, PV30668 (LxW = 0.67x1.52); P2 sin, PV30669 (LxW = 0.8x1.43); 2 fragments of I1, PV30670-PV30671.

Description

P2. Single-lobed tooth of variable occlusal outline with well-developed long paraflexus; hypercone sharpened, anteriorly with enamel hiatus; lagicone with undulated anterior enamel wall; in the former specimen (Figure 4.1) the posterior enamel wall of tooth and the anterior enamel wall of hypercone are both convex, in contrast to the latter one (Figure 4.2) with concave posterior enamel wall of tooth and hypercone with secondary protrusion.

Comparison and remarks. The availability of only two P2s from Tepe Alagöz makes a direct comparison with many taxa impossible. Moreover, this scarce material, without any p3s and/or mandibles, does not allow a definite specific/generic attribution. The first ochotonine occurrence in Asia Minor is dated to 9.9 Ma at Sinap Loc. 8A with Bellatonoides eroli (Şen, 2003). Compared to the material under study, P2 of B. eroli is of similar size, but morphologically seems to be different (based only on two P2s available; cf. Şen, 2003) in less-developed paraflexus and hypercone, without enamel hiatus. The oldest representatives of the genus Ochotona in the peri-Paratethyan area are O. ozansoyi Şen, 2003 from Sinap Loc. 84, Turkey and O. kalfense Lungu, 1981 from Kalfa, Moldova (Čermák, 2016); both dated to the late Vallesian (early MN10) [Şen, 2003; Čermák, 2016]. Both species differ from the Tepe Alagöz ochotonid in their larger size of P2, which have a nearly trapezoidal outline with a short paraflexus. Ochotona eximia (Khomenko, 1914) described from the late Miocene (middle Turolian, MN12) locality of Tarakliya (Moldova) is one of the largest species of the genus (Čermák, 2016). Estimated indirectly from p3 size (LxW = 2.2x2.0), it should be significantly larger than the taxon from Tepe Alagöz (Čermák, 2016). This is also true for all three species of the genus Pliolagomys Agadjanian and Erbajeva, 1983 (see Erbajeva, 1988; Erbajeva and Shushpanov, 1988; Čermák, 2010 for details). In size, the analyzed P2s are comparable with 1) Ochotona antiqua Argyropulo and Pidoplichka, 1939, well documented from the early Ruscinian (MN14) localities of Ukraine and Moldova (Erbajeva and Shushpanov, 1988; Čermák and Rekovets 2010) and 2) the slightly younger genus Ochotonoma Şen, 1998, well documented from the late Ruscinian (MN15) localities of Turkey, Bulgaria, Romania, and Hungary (Terzea, 1997; Ünay and de Bruijn, 1998; Şen, 1998, et al. 2019; Popov, 2004; Čermák, 2007). Ochotonoma also has very similar P2 morphology; in a number of P2 specimens, their lagicone is anteriorly undulated, and the hypercone possesses a secondary protrusion (see Terzea, 1997; Ünay and de Bruijn, 1998; Şen, 1998). Ochotona mediterranensis described by Suata-Alpaslan (2009c) from the contemporaneous (MN14) locality İğdeli has P2 slightly smaller (x̄: LxW = 0.64x1.18; N = 7), but unfortunately its morphology remains unclear. This species was also referred by Şen et al. (2017) from the early Ruscinian (MN14) locality of Ҫeştepe, sharing close similarities in size and tooth morphology with the İğdeli specimens. Ochotona sp. (O. mediterranensis sensu Suata-Alpaslan, 2009c and Şen et al., 2017) from Maritsa, Greece (MN13/14) seems to be, indirectly estimated based on p3 dimensions, smaller than ochotonine taxon from Tepe Alagöz, (cf. de Bruijn et al., 1970; Čermák, 2016). Unfortunately, no P2 is available from Ҫeştepe and Maritsa.

The only available P2 are most compatible with those in the above discussed Pliocene species of Ochotona and Ochotonoma. Unfortunately, the analyzed teeth do not bear sufficient diagnostic features and, therefore, it is impossible to determine the genus or species. Without further relevant ochotonid material from Tepe Alagöz they are tentatively assigned here as Ochotona seu Ochotonoma sp.

Family Leporidae Fischer, 1817
Subfamily Leporinae Fischer, 1817
Genus Trischizolagus Radulesco and Samson, 1967
Trischizolagus gambariani (Melik-Adamyan, 1986)
Figure 4.3-26, Table 1 

Nomeclatural remarks and lectotype designation. The species-group name gambariani was originally erected by Melik-Adamyan (1986) in the tentative, but unambiguous, combination with the generic name Alilepus (cf. Article 11.9.3.4 of ICZN, 1999). The species description fulfills the mandatory conditions of Article 13.1.1 (ICZN, 1999). The nominal species-group taxon was established based on the syntype (Article 73.2 of ICZN, 1999) consisting of 10 specimens with four p3s (Melik-Adamyan, 1986: 136, 137; figures 1-3). No single name-bearing type specimen was subsequently designated (lectotype [Article 74]).

In the sense of Articles 74.7 and 74.4 and Declaration 44, we hereby designate the left p3 figured (Article 74.4) in Melik-Adamyan (1986, p. 137, figure 3; Article 74.7.2) as a lectotype (Article 74.7.1 and Declaration 44) of the nominal taxon of Trischizolagus gambariani (Melik-Adamyan, 1986) described from the early Pliocene (MN14) locality Nurnus (Armenia).

Name-bearing type, type locality, and age. Lectotype (designated in this paper) - left p3 figured in Melik-Adamyan (1986, p. 137, figure 3); Nurnus (Armenia), early Pliocene (early Ruscinian, MN14).

Material. 1 I1 dex, PV30530; 1 I1 sin, PV30531; 4 fragments of I1, PV30542, PV30453, PV30560, PV30666; 3 I2, PV30637-PV30639; 2 P2 dex, PV30524, PV30525; 2 P2 sin, PV30523, PV30526; 1 fragment of P2, PV30541; 4 P3 dex, PV30617, PV30660-PV30662; 2 P3 sin, PV30618, PV30659; 5 P4/M1 dex, PV30608-PV30612; 2 P4/M1 sin, PV30606, PV30607; 2 M2 dex, PV30615, PV30616; 2 M2 sin, PV30613, PV30614; 4 fragmentary or juvenile M3, PV30640-PV30642, PV30667; 8 fragments of upper molariforms, PV30619-PV30626; 1 fragment of mandibular body dex with p3-m2, PV30528; 9 i1 dex, PV30532, PV30533, PV30534, PV30545, PV30546, PV30551, PV30655-PV30657; 7 i1 sin, PV30547-PV30550, PV30649, PV30653, PV30654; 7 fragments of i1, PV30552, PV30554-PV30557, PV30664, PV30665; 2 i1 juv, PV30553, PV30663; 7 p3 dex, PV30516-PV30520, PV30522, PV30529; 9 p3 sin, PV30509-PV30515, PV30521, PV30527; 8 fragments of p3, PV30535-PV30539, PV30544, PV30558, PV30559; 4 p4 dex, PV30565-PV30568; 6 p4 sin, PV30561-PV30564, PV30650, PV30658; 2 m1 dex, PV30573, PV30574; 5 m1 sin, PV30569-PV30572, PV30651; 3 m2 dex, PV30580-PV30582; 6 m2 sin, PV30575-PV30579, PV30652; 8 m3 dex, PV30630-PV30636, PV30648; 3 m3 sin, PV30627-PV30629; 5 fragmentary or juvenile m3, PV30643-PV30647;1 milk lower tooth, PV30605; 22 fragments of lower molariforms, PV30583-PV30604.

Measurements. See Table 1.

Description

i1. (Figure 4.5-6) Quadrangular, markedly prolonged anteroposteriorly; anterior enamel wall thick with constant thickness.

p3. (Figure 4.11-14, 15 [partim], 16-19, 24-24') Almost exclusively limited to PR2 pattern (presence of mesofossettid) associated with A1 pattern (presence of anteroflexid), in one case (Figure 4.11) PR2 pattern is associated with A0 pattern (absence of anteroflexid) and in one case (Figure 4.23) PR1 pattern (presence of mesoflexid) is associated with A1 - (A1/PR2 = 88%, A0/PR2 = 6%, A1/PR1 = 6%, N = 16); all teeth with stable pattern along the entire tooth crown, including one juvenile tooth (Figure 4.24-24'); depth of anteroflexid very variable from 0% (missing) to 18% (long) of L (average = 12%; N = 16); the anteroconid narrow, its length ranges from 25% to 33% of L (average = 30%; N = 16), size relationship between labial and lingual anteroconids is variable; protoflexid quite wide with variable angle between enamel walls, its depth varies from 13% to 20% of W (average = 17%; N = 15); a shallow paraflexid or concavity is present in 87% (N = 15) of specimens, and in six cases the notch is filled with cement; mesofossettid variable in its size and morphology; hypoconid massive, its labial side, predominantly deformed anterolabially by a depression (morphotype “c” [sensu Čermák, 2009]; 76%, N = 17); hypoflexid not crenulated, reaching about half width of the crown (min-x̄-max [%] of W is 48-53-59%), its lingual end simple - predominantly of morphotype “A” (sensu Fladerer and Reiner, 1996; 41%, N = 17) and morphotype “B” (sensu Fladerer and Reiner, 1996; 35%, N = 17).

Lower molariforms. (Figure 4.15 [partim]) Trigonid - in relation to talonid - small with smooth anterobuccal corner (no flexid present); labial part of the talonid anterolabially concave; isthmus between trigonid and talonid thin and long; flexid between trigonid and talonid smooth; very thick enamel on the labial part of the tooth and on the trigonid posterior edge.

m3. (Figure 4.20) Typically bean-shaped trigonid, larger and wider than the oval talonid, the both with thicker enamel on labial sides.

I1. (Figure 4.3-4) Occlusal outline of irregular quadrangle, anteriorly prolonged in its medial part; anterior enamel thin with no substantial variation; anterior notch shallow, V-shaped with widely opened walls, not filled with cement; anterior notch divides the tooth in two parts of approximately equal anterior prominence, the medial one (~46% of W).

P2. (Figure 4.7-10) Occlusal outline oval; paraflexus short, its length on average 56% (N = 4) of tooth length; hypercone advanced, with relatively long hypoflexus of LL-morphotype between V and VI (sensu Fladerer and Reiner, 1996); lagicone with moderately developed mesoflexus of BMR-morphotype B (sensu Fladerer and Reiner, 1996).

Upper molariforms. (Figure 4.25-26) Hypostria quite short, markedly crenulated, with abundant cement lingually; typically thicker enamel on the anterior part of the anteroloph and the lingual tips of posteroloph; relatively thin enamel in the anterior part of the anteroloph.

Comparison and remarks. The leporid from Tepe Alagöz is attributed here to the genus Trischizolagus Radulesco and Samson, 1967 for showing the following combination of discriminant features: 1) the presence of anterofelxid in p3 (= A1 morphotype; in 94%, N = 17), 2) the presence of short hypoflexid associated with mesofossettid (= PR2 morphotype; in 94%, N = 16), and 3) the exclusive presence of simple - uncrenulated - flexids in lower teeth. This discriminates the leporid under study from Old World: 1) species of Hypolagus Dice, 1917 which bear A0/PR0 p3; 2) species of Serengetilagus Dietrich, 1941 with A0-1/PR0 p3; 3) species of Alilepus Dice, 1931 bearing A0/PR1-2 p3; 4) species of Pliopentalagus Gureev and Konkova in Gureev, 1964 which have crenulated flexids in lower teeth; and 5) species of Lepus Linnaeus, 1758 and Oryctolagus Lilljeborg, 1874 bearing A1/PR3 p3.

In p3 morphology the leporid from Tepe Alagöz is fully compatible with the stratigraphically and geographically close species T. gambariani described from the contemporaneous (MN14) locality of Nurnus (Armenia). In addition to the significant presence of a PR2 p3 pattern (Figure 5), both species share also the 1) variable depth and morphology of p3 anteroconid, 2) well-manifested concavity or even shallow paraflexid in the anterolingual enamel wall of p3, and 3) hypoconid deformed anterolabially by a depression. The measurements of p3s under study fit in the upper range of the dimensional variability of those in type series of T. gambariani (Figure 6).

Trischizolagus crusafonti (Janvier and Montenat, 1971) - (La Alberca, Spain; MN 13) and T. maritsae de Bruijn et al., 1970 - (Maritsa, Greece; MN 13/14), both representing the early species of the genus, differ from the taxon under study in its smaller size of p3 (Figure 6) and missing mesofossettid in p3 (i.e., the presence of PR0 and/or PR1 p3 pattern(/s); Figure 5). Nevertheless, it is worth noting that in the case of T. maritsae, dimensions of p3 are not easily comparable because the teeth apparently come from subadult individuals (de Bruijn et al., 1970).

Trischizolagus dumitrescuae Radulesco and Samson, 1967, described from the early Pliocene (MN15a) locality of Măluşteni and reported from many Pliocene (MN14-16) localities from southeastern and eastern Europe (Čermák and Wagner, 2013), shows considerable variation in size and morphology of P2/p3. Nevertheless, the species differs from the Tepe Alagöz leporid in its significant predominance of PR1 p3 pattern (PR0 = 3.4%, PR1 = 68.4%, PR2 = 28.2; N = 131 [9 MN14-15 localities]; see Figure 5 for details) and its predominantly simpler P2 (in ca. 70% of 25 cases; Topachevsky, 1980; Averianov and Tesakov, 1997 and data herein). The p3 and P2 size of taxon under study do not exceed the size range observed in T. dumitrescuae (see Čermák and Wagner, 2013); in relation to the type series of T. dumitrescue, the available p3s from Tepe Alagöz fit in the lower range of the type series or slightly below (Figure 6). Incisors, both upper and lower, in T. dumitrescuae are anteroposteriorly more elongated that those in T. gambariani (cf. Averianov, 1995); the feature is more expressed in the upper one (L/W is 0.70 for T. g. vs 0.84 for T. d.; Averianov, 1995, and data herein).

Trischizolagus mirificus described by Qiu and Storch (2000) from the early Pliocene (MN14) locality of Bilike (Inner Mongolia, China) differs from the taxon under study in its considerably simpler (“Hypolagus-like”) morphology of p3 (PR0 pattern in 77% of cases; the pattern with mesofossettid (PR2) absents; N = 25; Qiu and Storch, 2000). P2 occlusal outline of T. mirificus is also simple, generally of LL-morphotypes I-III and BMR-morphotypes 0-A in contrast to LL-morphotype V/VI and BMR-morphotype B in the material under study. Both taxonomically significant teeth in T. mirificus are smaller than those in the material under study (Figure 6, Table 1, Qiu and Storch, 2000).

Trischizolagus nihewanensis (Cai, 1989), originally referred to Pliopentalagus, was erected based on one p3 and two lower molariform teeth coming from the lower part of the Daodi Formation (late Pliocene) of Yangyuan and Yuixian (Hebei Province, China). The only available p3 differs from the taxon under study in its PR1 p3 pattern and its more infolded enamel walls in posterior structures of teeth. According to Tomida and Jin (2005), the p3 of T. nihewanensis is characterized with the most complicated enamel pattern within the genus. The p3 size of T. nihewanensis is similar to those in leporid from Tepe Alagöz (Figure 6).

It is worth mentioning here the leporid findings supposedly related to Trischizolagus (in Şen, 1983 and Averianov and Tesakov, 1997; Pliopentalagus sp. and/or Serengetilagus sp. in Şen and Erbajeva, 1995) from the early Pliocene (cf. MN14) locality of Pul-e Charkhi locality, Afghanistan (Şen, 1983). The available two p3s (one fragmentary) do not allow an evaluation of variation. Nevertheless, they differ from the specimens under study in their smaller size (LxW = 3.05 x 2.90, - x 2.96 mm; measurements of SČ). The fragmentary p3 of Pul-e Charkhi, referred by Şen and Erbajeva (1995, figure 1a) to Pliopentalagus sp., differs also in more infolded posterior walls in talonid structures. In the second p3 of Pul-e Charkhi, possessing the A1/PR0 pattern, (AFG 759, SČ pers. obs; referred to Trischizolagus cf. maritsae in Şen, 1983; Trischizolagus sp. in Averianov and Tesakov, 1997; Serengetilagus sp. in Şen and Erbajeva, 1995) the mesofossettid is present. Nevertheless, this mesofossettid is located very close to the medial end of the hypoflexid, and is much smaller and rounder than those in Tepe Alagöz leporid (Figure 4).

Other questionable leporid findings compatible with the attribution to Trischizolagus, originally described by Geraads (1994) as Serengetilagus raynali, are known from the Pleistocene locality of Rhino Cave in Morocco. The leporid is similar to the taxon under study in its exclusive appearance of the mesofossettid (A1/PR2/Pa1 p3 pattern), but it differs in its very short and wide anteroconid of p3 (in two of four) and significantly smaller p3 (L x W of p3: OR = 2.53-2.90 x 2.41-2.74, M = 2.62 x 2.55: N = 4; Geraads, 1994). Unfortunately, based on the available material the precise generic attribution is still impossible.

Emended diagnosis. Medium-sized leporid possessing: 1) p3 almost exclusively limited to p3 of A1/PR2 pattern with narrow anteroconid and very variable anteroflexid associated with P2 bearing short paraflexus, relatively long hypoflexus of LL-morphotype between V and VI, and moderately developed mesoflexus of BMR-morphotype B; 2) anteroposteriorly shortened I1 with shallow V-shaped cement free anterior notch; 3) uncrenulated flexids in lower teeth.

The above combination of features discriminates T. gambariani from: 1) species of Hypolagus bearing A0/PR0 p3; 2) species of Serengetilagus bearing A0-1/PR0 p3; 3) species of Alilepus bearing A0/PR1-2 p3; 4) species of Pliopentalagus bearing crenulated flexids in lower teeth; 5) species of Lepus and Oryctolagus bearing A1/PR3 p3; 6) “Trischizolagus” raynali bearing significantly smaller p3 with shorter and wider anteroconid; and 7) Trischizolagus crusafonti, T. dumitrescuae, T. maritsae, T. mirificus, T. nihewanensis bearing, exclusively or predominantly, A1/PR0-1 p3 and P2 (if available) with LL-morphotype 0-IV. Moreover, T. crusafonti, T. maritsae, T. mirificus differ in their significantly smaller p3 and T. dumiterescuae in its more anteroposteriorly elongated I1.

Stratigraphic and geographic distribution. Early Pliocene (Ruscinian, MN14); southern regions of peri-Paratethyan area, currently Turkey and Armenia [localities Nurnus (AM, MN14, type locality), Tepe Alagöz (TR, MN14)].

DISCUSSION AND CONCLUSIONS

Tepe Alagöz: Age of the Assemblage

Biochronologic interpretation of the rodent assemblage from Tepe Alagöz is rather tricky because our rodent material is scarce. Occitanomys debruijni appears together with Pseudomeriones hansi in Anatolia only in the locality of İğdeli (de Bruijn et al., 2013; Suata-Alpaslan, 2009a). On the other hand, Allocricetus cf. bursae from İğdeli slightly differs from our A. cf. ehiki. Moreover, the arvicolids are already present in the assemblage from İğdeli while they are absent in the assemblage from Tepe Alagöz. This is, of course, only indirect evidence because their absence may reflect a small sample size. Nevertheless, the Tepe Alagöz rodent assemblage seems to be of about the same age or somewhat older than İğdeli and, thus, represents a time slice close to Miocene/Pliocene transition. In terms of local biozonation, the age of the assemblage from Tepe Alagöz can be interpreted as local zone M that is tentatively correlated to biounit MN14 in Europe (de Bruijn et al., 2013). This is in good accordance with the lagomorph taxa recorded in this locality.

Leporids of Tepe Alagöz: Taxonomy and Paleobiogeography

The almost exclusive occurrence of anteroflexid together with mesofossettid in the p3 phenotype (i.e., A1/PR2) clearly allows an attribution of leporid material from Tepe Alagöz to the genus Trischizolagus (cf. Radulesco and Samson, 1967; Averianov, 1995; Averianov and Tesakov, 1997; López Martínez et al., 2007; Čermák and Wagner, 2013). Nevertheless, the presence of mesofossettid in 94% of cases (N = 16) is quite unusual among the known Pliocene records of this genus. The fossil record of the earliest species of Trischizolagus represented by T. crusafonti (La Alberca, Spain, MN13) and T. maritsae (Maritsa, Greece, MN13/14) is, unfortunately, very scarce and prevents any reliable evaluation of p3 morphotype composition and thus any conclusive comparisons. Available p3s lack a mesofossettid (Figure 5; cf. de Bruijn et al., 1970; Janvier and Montenat, 1971). Note that an atypical weak lingual flexus observed in both available p3s of T. crusafonti from the type locality do not allow clear recognition of a mesoflexid (cf. López Martínez et al., 2007). Nevertheless, p3 of the species is generally attributed to PR0 pattern (e.g., in Averianov and Tesakov 1997; López Martínez et al., 2007; Čermák and Wagner, 2013; this paper, see Figure 5). The mesofossettid has not been documented in either T. mirificus (Bilike, China, MN14) or in T. nihewanensis (Yangyuan-Yuxian, China, MN16). The available p3s of T. crusafonti, T. maritsae, and T. mirificus generally have a rather simple or primitive appearance, and the phenotype composition in their fossil record suggests the presence of a PR0 p3 pattern (Figure 5). The only available p3 of much younger T. nihewanensis is of PR1 p3 pattern (Figure 5) with relatively advanced traits with undulation of flexids (Cai, 1989; Tomida and Jin, 2005).

The best known and understood species of the genus is Trischizolagus dumitrescuae documented from almost 20 early Pliocene localities of Hungary, Romania, Bulgaria, Greece, Moldova, and southern Ukraine (Radulesco and Samson, 1967, 1995; Topachevsky, 1980, 1987; Averianov and Tesakov, 1997; Popov, 2004; Čermák and Wagner, 2013). No reliable record of the species has been reported from pre-MN14 localities; all of these findings still remain questionable (e.g., Kovalchuk et al., 2017). In the early Ruscinian (MN14) T. dumitrescuae, the PR1 p3 pattern significantly predominates over the PR2 one (66% vs. 28% respectively; N = 109), whereas the PR0 p3 pattern is very rare and is present in 6% of cases (Čermák and Wagner, 2013). During the late Ruscinian (MN15) no significant changes in p3 pattern composition can be observed in the record of T. dumitrescuae; the PR1 is available in 68%, PR2 in 29%, and PR0 in 3% of cases (N = 34; Čermák and Wagner, 2013, updated). The p3 morphotype compositions of more numerous samples of the species from particular localities are shown in Figure 5. The presumed last appearance most probably belonging to T. dumitrescuae (here classified as Trischizolagus sp. - following Averianov and Tesakov, 1997) comes from the early Villányian (early MN16) locality Obukhovka 2 (Russia, Rostov Region).

The available material of Trischizolagus from Nurnus (MN14) originally described by Melik-Adamyan (1986) as “Alilepus” gambariani was reassigned as T. dumitrescuae by Averianov and Tesakov (1997; contra Čermák and Wagner, 2013). But, although scanty (four p3), its phenotype composition does not fit into the well-documented one of T. dumitrescue, where PR1 clearly predominates. Even in other comparably scanty samples of T. dumitrescue, the exclusive presence of PR2 specimens has never been documented (Figure 5). It could have been assumed until now that the exclusive presence of the PR2 morphotype could be a result of taphonomic influences (e.g., prey accumulations). But the new material from Tepe Alagöz described here strongly suggests that the uncommon p3 pattern composition recorded in Nurnus is not an accidental phenomenon and that leporids from these coeval localities represents one species, distinct from T. dumitrescuae.

The available fossil record of Trischizolagus indicates that the northwestern part of the peri-Paratethyan area can be regarded as the core distribution area of T. dumitrescuae. Most known findings of this species reported from there are correlated with the early Ruscinian, and more western occurrences (i.e., from Muselievo (BG) or Beremend (H)) are limited to the late Ruscinian (Čermák and Wagner, 2013). South and southeastern parts of the peri-Paratethyan areas, on the other hand, were most probably inhabited by distinct T. gambariani, referred from MN14 localities of Nurnus (AM) and Tepe Alagöz (TR). It cannot be excluded that the somewhat younger Trischizolagus reported by Ünay and de Bruijn (1998) from Tozaklar (MN15) also belongs to this species, but the scarcity of material does not allow a definite specific determination. Leporids from Babadat (MN14), Akçaköy (MN14), and Tekman (MN15) referred by Suata-Alpaslan (2010, 2012) to Pliopentalagus are reported only in faunal lists without any descriptions or images.

The taxonomy of the geographically close leporid recorded from Maritsa (Rhodos, Greece) has not been fully resolved. The age of the locality is near the Miocene/Pliocene boundary, but there is no consensus on its precise stratigraphic position; it is predominantly correlated with the early MN14 (e.g., de Bruijn et al., 1970; van der Meulen and van Kolfschoten, 1986; Koufos, 2006; Şen et al., 2017), less often with the late MN13 (e.g., Doukas, 2005; Hordijk and de Bruijn, 2009). In our view, it is not possible to give any conclusive argument to support one of the above views for now, thus the age attribution near the MN13/14 boundary is preferred and used here for this locality. Maritsa does appear to be older than Tepe Alagöz and İğdeli. The leporid from Maritsa is commonly regarded as a primitive species within Trischizolagus. With its occlusal p3 outline possessing a less-developed lingual anteroconid and poorly developed lingual structures, the leporid from Maritsa is similar to Trischizolagus crusafonti, hitherto known only from its type locality (La Alberca, S Spain; MN 13). Similar features are also recognizable in the leporid remains from the nearby locality of Alcoy N (MN13), referred by López Martínez (1989) as T. cf. maritsae; the taxon was also reported by the author from the MN13-14 localities Salobreña, Caravaca, and Gorafe 1, but the scarcity of the material from these localities prevents any reliable comparison and taxonomic evaluation. Unsurprisingly, Erbajeva and Angermann (1983) and López Martínez et al. (2007) also point out similarities between the leporid from Maritsa and Serengetilagus praecapensis (the taxon with very low potential to develop lingual structures in p3). This view is also supported by our observations, particularly of leporids from MN13/14 locality of Wádí Natrún (N Egypt; Studer, 1899; Andrews, 1902) representing the African finding, well-assignable to Serengetilagus (Čermák, unpubl. data), geographically nearest to Maritsa. That may indicate an African affinity of the Maritsa leporid. For sake of completeness, it is worth noting in this context that the sporadic single p3 specimens (AFG 759, AMNH 21617) from the early Pliocene localities of Pul-e Charkhi (Afghanistan; Şen, 1983, Şen and Erbajeva, 1995) and Kholobolchi Nor C (Mongolia; Flynn and Bernor, 1987) also possess a similar Serengetilagus-like appearance.

In summary, the leporid from Tepe Alagöz is well co-identifiable with the nominal taxon of T. gambariani and not with that of T. maritsae, even though the type materials of the both taxa are not fully satisfactory. Based on the available fossil record and present state of our knowledge it is not possible to prove that leporids from Nurnus and Maritsa represent one species. The available data suggest the opposite.

The p3 Mesofossettid in Leporidae: An Unsolved Mystery

The presence and evolution of mesofossettid during Old World leporid history was reviewed in detail by Čermák et al. (2015). The oldest Old World evidence of a frequent mesofossettid in p3 is documented from the middle-late MN12 of north-western peri-Paratethysian area in Alilepus laskarewi (Čermák et al., 2015). In this genus the presence of mesofossettid, but significantly less common, can also be observed in A. longisinuosus (Lufeng, Yunnan, China; MN12/13; Qi et al., 2006) and sporadically also in A. annectens (Ertemte 2, China; MN13; Qiu, 1987). Among other Eurasiatic leporid taxa the mesofossettid shows a high incidence only in Pliopentalagus species; within the latest Miocene - late Pliocene lineage P. huainanensis Jin, 2004 - P. dajushanensis Tomida and Jin, 2009 - P. anhuiensis Tomida and Jin, 2009 the p3 mesofossettid is gradually reduced in relation to the mesoflexid (in more detail in Tomida and Jin, 2009; Čermák et al., 2015). The only European record of this genus is the early Pliocene (MN15) P. dietrichi (Fejfar, 1961), which p3 shows an exclusively PR1 morphotype.

In addition, there are a number of Old World leporid fossils of unsure species/genus attribution, where p3 mesofossettids are also seen. The small enamel lake (?mesofossettid) located close to the medial end of hypoflexid is observable in the poorly preserved p3 (AFG 759; SČ, pers. obs.) from the early Pliocene (MN14) Pul-e Charkhi locality, Afghanistan (referred to Trischizolagus cf. maritsae in Şen, 1983; Trischizolagus sp. in Averianov and Tesakov, 1997; Serengetilagus sp. in Şen and Erbajeva, 1995). In the latest Pliocene and early Pleistocene of China there is a group of leporids in which the stable p3 mesofossettid (/enamel lake), of different morphology and location, is associated with the simple p3 anteroconid (A0/PR2 p3 morphotype). This p3 morphotype has generally been found together with teeth of A0/PR0 or A0/PR1 morphotype. Taxonomy of these leporids is still poorly understood, and their generic attribution still remains unclear. These have generally been identified with the species brachypus described by Young (1927) and originally assigned in the genus Caprolagus. The type material was referred by various authors to different genera: to Hypolagus by Schreuder (1937), to Alilepus by Gureev (1964) - followed by Cai (1989), to Sericolagus by Averianov (1996; erected as new) - followed by Wu and Flynn (2017), to Brevilagus by Zhang, Z.-Q. (2001; the junior objective synonym of Sericolagus). Over the past several decades, findings considered to be related to this species (reported under various generic assignment) have been reported from China including - Loc. 2 of Gaojiaya, Jingle (Teihard de Chardin and Young,1931); Loc. 22 of Shouyang (Young, 1935); Loc. 18 (Teilhard de Chardin, 1940); Yushe (Teilhard de Chardin, 1940; Wu and Flynn, 2017); Heshui of Gansu (Zheng, 1976); Jinniushan of Liaoning (Zhang, S.-S., 1993); the East and West Caves near Zhoukoudian (Cheng et al., 1996); Sunjiashan of Zibo (Zheng et al., 1997); Ningyang (Zhang, Z.-Q., 2001); Fanchang, Anhui (Jin and Xu, 2009).

It is worth mentioning in this context the questionable leporid findings from the Pleistocene locality Rhino Cave in Morocco originally described by Geraads (1994) as Serengetilagus raynali. The exclusive presence of the mesofossettid and predominantly very wide anteroconid in p3 strongly support the view by Şen and Erbajeva (1995), Averianov and Tesakov (1997), and López Martínez et al. (2007), which put the Moroccan leporid apart from the African taxa referred to Serengetilagus. Averianov and Tesakov (1997) referred these specimens as Trischizolagus sp., but the presence of a markedly square outline of p3 with very short and wide anteroconid and distinctly young age of these findings do not fully support an attribution to this genus. The features are rather typical for Oryctolagus.

A predisposition to development of this structure has been available already in the earliest forms of Leporinae (Čermák et al., 2015); the initial appearance is recorded from the middle Miocene (late Barstovian) of North America (Voorhies and Timperley, 1997). Based on the leporid record discussed above, together with well-documented one of North America (Dawson, 1958; White 1988, 1991), we can conclude that the presence of mesofossettid (/enamel lake) in leporid p3 is a relatively common phenomenon. It is well associated with both A0 and A1 p3 anteroconid type (i.e., with anteroflexid or without it) in various ratios and morphologies across genera. Taxonomically significant differences related to this structure can often be found on the species level.

Hypolagus, a widespread and well understood genus of Archaeolaginae, rarely has similar tooth structures (Fladerer and Reiner, 1996). If present, the enamel lake is generally small and simple, located close to the medial end of hypoflexid, and often is not present along the entire tooth shaft. Most likely the lake was derived from the medial end of hypoflexid or even accidentally, independently to any adjoining structures (Čermák et al., 2015). This could be the case of leporid p3 from Pul-e Charkhi (Şen, 1983; Şen and Erbajeva, 1995) and also Sericolagus yushecus (Wu and Flynn, 2017: figure 4.10b). In Leporinae, a predisposition to development of posterolingual tooth structures together with anteroflexids is significantly higher. These structures appear across the Leporinae lineage in various combinations and ratios and often are taxonomically discriminative for numerous species and genera (Hibbard, 1963; White, 1991; Čermák et al., 2015).

So, the available fossil record in many leporid lineages suggests different origins of enamel lake in p3 (Čermák et al., 2015). Moreover, even within Leporinae clade the p3 PR1/PR2 changes over time in different lineages show different morphoclines, compare e.g. lineage Alilepus => Nekrolagus => Lepus / Sylvilagus (Hibbrad, 1963; Averianov and Tesakov, 1997) vs above mentioned east Asiatic lineage of Pliopentalagus species (Tomida and Jin, 2009). Thus a generally accepted Hibbard (1963) hypothesis proposing the development of posterointernal structures of p3 in the sequence mesoflexid => mesofossettid has a limited validity (Čermák et al., 2015). In this perspective, it is also not surprising that development of the anteroflexid is a phenomenon that appeared independently several times in different lineages (White, 1991).

ACKNOWLEDGMENTS

We would like to thank to M. Kováčová, I. Mazzini, and M. Poliak for their help during the field campaign. We thank also four anonymous reviewers for valuable comments and critical remarks. SČ has been supported by institutional support RVO67985831 of the Institute of Geology of the Czech Academy of Sciences. PJ has been supported by VEGA 1/0702/17 and Slovak Research and Development Agency (SRDA) Grant APVV-15-0575.

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