20 Oct 2015: Tanaka Y, Kohno N (2015) Correction: A New Late Miocene Odobenid (Mammalia: Carnivora) from Hokkaido, Japan Suggests Rapid Diversification of Basal Miocene Odobenids. doi: info:doi/10.1371/journal.pone.0141406 View correction
The modern walrus, Odobenus rosmarus, is specialized and only extant member of the family Odobenidae. They were much more diversified in the past, and at least 16 genera and 20 species of fossil walruses have been known. Although their diversity increased in the late Miocene and Pliocene (around 8–2 Million years ago), older records are poorly known. A new genus and species of archaic odobenid, Archaeodobenus akamatsui, gen. et sp. nov. from the late Miocene (ca. 10.0–9.5 Ma) top of the Ichibangawa Formation, Hokkaido, northern Japan, suggests rapid diversification of basal Miocene walruses. Archaeodobenus akamatsui is the contemporaneous Pseudotaria muramotoi from the same formation, but they are distinguishable from each other in size and shape of the occipital condyle, foramen magnum and mastoid process of the cranium, and other postcranial features. Based on our phylogenetic analysis, A. akamatsui might have split from P. muramotoi at the late Miocene in the western North Pacific. This rapid diversification of the archaic odobenids occurred with a combination of marine regression and transgression, which provided geological isolation among the common ancestors of extinct odobenids.
Citation: Tanaka Y, Kohno N (2015) A New Late Miocene Odobenid (Mammalia: Carnivora) from Hokkaido, Japan Suggests Rapid Diversification of Basal Miocene Odobenids. PLoS ONE 10(8): e0131856. doi:10.1371/journal.pone.0131856
Editor: Matthew C. Mihlbachler, NYIT College of Osteopathic Medicine, UNITED STATES
Received: February 27, 2015; Accepted: June 8, 2015; Published: August 5, 2015
Copyright: © 2015 Tanaka, Kohno. This is an open access article distributed under the terms of the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original author and source are credited
Data Availability: The data matrix for the phylogenetic analysis is available both in NEX and TNT formats in the supporting information files. All character and modification lists are in word files.
Funding: Field and lab work were supported by the Department of Geology and Paleontology, National Museum of Nature and Science.
Competing interests: The authors have declared that no competing interests exist.
A partial skeleton of a fossil pinniped was collected from the late Miocene Ichibangawa Formation in Tobetsu Town, Hokkaido, Japan (Figs 1 and 2). This skeleton includes a partial cranium, mandibles, anterior vertebrae and some appendicular bones. Previously, the holotype and paratype of the extinct odobenid, Pseudotaria muramotoi Kohno, 2006, were collected from the same formation in the same locality area. The new fossil has similar character combinations to those in P. muramotoi, suggesting that it also belongs to the family Odobenidae. However, the third specimen has some unique characters differentiation it from the previously known specimens of P. muramotoi from the same locality area and also other species in the Odobenidae. In the present paper, we describe the new fossil as a new genus and species of the family Odobenidae and examine its phylogenetic relationships among them to provide additional information and understand the evolutionary diversification of the odobenids during the Miocene.
No permits were required for the described study, which complied with all relevant regulations.
The electronic edition of this article conforms to the requirements of the amended International Code of Zoological Nomenclature, and hence the new names contained herein are available under that Code from the electronic edition of this article. This published work and the nomenclatural acts it contains have been registered in ZooBank, the online registration system for the ICZN. The ZooBank LSIDs (Life Science Identifiers) can be identified and the associated information viewed through any standard web browser by appending the LSID to the prefix "http://zoobank.org/". The LSID for this publication is: urn:lsid:zoobank.org:author:E500AA1E-C47F-48C5-9A9D-9B8C0959E8FE. The electronic edition of this work was published in a journal with an ISSN, and has been archived and is available from the following digital repositories: PubMed Central, LOCKSS.
MAMMALIA Linnaeus, 1758
CARNIVORA Bowdich, 1821
ODOBENIDAE Allen, 1880
Archaeodobenus gen. nov.
Archaeodobenus akamatsui sp. nov.
As for the only species.
The generic name, Archaeodobenus, is named in Greek archaios meaning ancient, and the type genus name of the family Odobenidae.
Known from the late Miocene (ca. 10.0–9.5 Ma), Japan.
Archaeodobenus akamatsui sp. nov.
(A) dorsal view, (B) left lateral view, (C) ventral view.
(A) dorsal view, (B) left lateral view, (C) ventral view.
(A)—(C) left mandible, (D)—(E) right mandible, (A) lateral view, (B) dorsal view, (C) medial view, (D) lateral view, (E) medial view.
(A) left ceratohyoid, (B) basihyoid, (C) right ceratohyoid, (D) left thyrohyoid.
(A)—(D) Archaeodobenus akamatsui, (E)—(H) Pseudotaria muramotoi, (A) and (E) anterior view of the atlas, (B) and (F) left lateral view of the atlas, (C) and (G) anterior view of the axis, (D) and (H) left lateral view of the axis.
(A) lateral view of right scapula, (B) lateral view of right humerus, (C) lateral view of left scapula, (D)—(H) left lateral view of the cervical vertebrae, (D) third, (E) fourth, (F) fifth, (G) sixth, (H) seventh, (I)—(O) left lateral view of the thoracic vertebrae, (I) first, (J) second, (K) third, (L) fourth, (M) fifth, (N) sixth, (O) seventh.
Brackets indicate measurements explained by Sivertsen (1954:18–20).
Archaeodobenus akamatsui is an archaic odobenid with a slender and small cranium and non-tusked, moderate-sized upper canine. Distinguished from other archaic odobenids (Prototaria primigena, P. planicephala, Proneotherium repenningi, Neotherium mirum, Kamtschatarctos sinelnikovae and Pseudotaria muramotoi) by the following derived characters: pentagonal basioccipital (character 30), blade-like spinous process of axis (character 91). Distinguished from later diverging odobenids (Imagotaria downsi, Pontolis magnus, dusignathines and odobenines) by retention of the following primitive characters: deep mandibular fossa (character 26); small mastoid process (character 33); two distinct roots on premolars (expect P1) (character 74 and 76).
UHR 33282: Hokkaido University Museum, associated partial skeleton including a partial cranium (mostly left half) with left and right I3, right C, right P2, a left mandible with canine, a partial right mandible with incomplete canine, a basihyoid, a left thyrohyoid, ceratohyoids, nearly complete atlas, axis, cervical vertebrae 3–7, incomplete thoracic vertebrae 1–8, a left rib, three right ribs, an incomplete sternebra, partial scapulae, and nearly complete right humerus.
UHR 33282 was collected as a float near the Rutaka Bridge on the Tobetsu River by staff of the Tobetsu Town Board of Education. It is 1.5 km south and also down stream from Aoyama dam in Tobetsu-cho, Ishikari-gun, Hokkaido, Japan (43°27’34” north latitude and 141°35’35” east longitude) (Fig 2).
Formation and Age.
UHR 33282 was enclosed in a weathered, dark green fine-grained, massive consolidated glauconitic sand stone block as a float, originally from the glauconite bed from the top of the Ichibangawa Formation. Although the Lower Pliocene Tobetsu Formation is exposed at the locality , it is very different from the matrix adhering to the new fossil, suggesting that the block was transported from the upstream of the river. Three formations (the Morai, Ichibangawa and Ponsubetsu Formations) are exposed further upstream the Tobetsu River (Fig 2) . But these formations are silt, except the Ichibangawa Formation that is sandstone. In addition, the rich-occurrence of glauconitic sandstone with marine fossils and carbonates is known only in the upper part of the Ichibangawa Formation in this area (Kakimi and Uemura ), as shown by the gray band in Fig 2. Thus, the origin of UHR 33282 is the glauconite bed on the top of the Ichibangawa Formation.
Recognition of the glauconite bed is disputed. Kakimi and Uemura  described the bed as the uppermost of the Ichibangawa Formation. The Kabato Collaborative Research Group  and Takano et al.  recognized the bed as the lowermost part of the Morai Formation. On the other hand, Takano et al.  recognized as a separate unit and did not include it in both the Ichibangawa and Morai Formations. The lithology of the matrix, fine-grained, massive hard sand stone is similar to the Ichibangawa Formation (sandstone), rather than the Morai Formation (shale siltstone). In short, here, we follow the oldest study; i.e., Kakimi and Uemura , to recognize the fossil odobenid’s original formation, and also follow the estimated age of the glauconite bed of Takano et al. .
As Fig 2 shows the age of the Ichibangawa Formation is lacking. However, the overlying Morai Formation includes the Denticulopsis katayamae diatom zone, 9.2–8.5 Ma . Also, the underlying Subetsu Formation has a fission track age of 13±1 Ma by Tsuji , but it is not exposed at the locality . Based on these chronological information, Takano et al.  estimated the age of the Ichibangawa Formation (except the glauconite bed) to be approximately 11.5–10 Ma, and they also considered the uppermost glauconite bed of the Ichibangawa Formation to be around 10–9.5 Ma based on previous studies.
The species is named in honor of Dr. Morio Akamatsu, a curator emeritus of the Hokkaido Museum, for his longstanding contributions to geology and paleontology of Hokkaido, and in gratitude for his encouragement and assistance to both of us throughout this study.
Gender and ontogenetic age
The nine cranial sutures that Sivertsen  considered to be useful to evaluate relative ontogenetic ages of otariid pinnipeds, at least six are nearly closed. This indicates that the new fossil belongs in Sivertsen’s Group II age class (i.e., subadult). In addition, well developed lambdoidal crests and relatively large canines suggest that the animal represents a male.
Estimated body size.
The estimated body size of the holotype individual is 2.8–3 m in total length and 390–473 kg in total weight. Holotype of A. akamatsui is an intermediate size between modern male Eumetopias jubatus (3.3m, 1000kg) and Otaria flavescens (2.6 m, 300–350 kg) (Jefferson et al. ).
The body size of Archaeodobenus akamatsui can be inferred by the method of Churchill et al. , using formulae for the Otariidae (S1 File). The holotype cranium of A. akamatsui shows similar proportion with otariids rather than highly specialized modern walrus Odobenus rosmarus. On the holotype of A. akamatsui, the posterior end of the palatine is missing, which is used as a landmark to apply the formulae. Here, we took two measurements for the palatine length from the prosthion to the most posterior preserved point of the palatine and the most anterior preserved point of the hamular process base. Thus, the estimated body length and mass are presented as a range of possible body size.
The occipitals are preserved mainly on the left side of the cranium. The basioccipital is broad posteriorly and trapezoidal in shape. The muscular tubercle for the origin of the longus and rectus capitis muscles is well developed anterolaterally on the midportion of the basioccipital. The portion posterior to this tubercle bears a deep and anteroposteriorly long hemispherical fossa. The jugular (posterior lacerate) foramen is large (12.0 mm long and 11.2 width) and crescentic in shape, but this might be a result of deformation, a weak slide to the medial. The hypoglossal foramen is relatively large, and its diameter is 4.6 mm. The occipital condyles are transversely narrow and dorsoventrally high, and are projected weakly posteriorly. The medial margins of the occipital condyles from posterior view are nearly vertical. The foramen magnum is dorsoventrally deep and elliptical in shape. The dorsal and ventral condyloid fossae are deep. A pair of crests (around 20 mm length) rise up from the medial side of the occipital condyles to the middle, on the dorsal margin of the foramen magnum uniquely (Fig 5). The jugular process is short, mediolaterally thin, and plate-like in structure. The suture between the jugular process and mastoid process is not fused. The nuchal tubercle is very weak. The occipito-squamosal suture is almost fused. The lambdoidal crest is thick and posterodorsally projected.
The left squamosal is nearly complete, but missing the anterior part of the slender zygomatic process. The pseudosylvian sulcus is weakly present, and it is located just above the temporal fossa. The temporal fossa, between the braincase and the zygomatic process, is relatively wide, smooth and is continued posteriorly to the dorsal surface of the laterally projected mastoid process, so that the temporal fossa has an anteroposteriorly extended flat floor of 38.3 mm in length. The mandibular fossa is subcylindrical, and it makes a deep groove dorsally. The retroglenoid process is a transversely wide and anteroposteriorly thin plate, which projects strongly anteroventrally and forms deep mandibular fossa. The mastoid process is relatively small and projected laterally. Its lateral surface for the origins of the sternomastoideus and cleidomastoideus muscles is smooth probably because of the young age of the holotype individual.
The ventral surface of the tympanic bulla is inflated and smooth. The tympanic bulla is comprised mostly of ectotympanic and delimited anterolaterally by the posteromedial side of the retroglenoid process and posterolaterally by the anteromedial side of the mastoid process. An anterior part of the bulla has a mediolaterally elongated shallow depression, just posterior to the retroglenoid process. The external acoustic meatus is relatively large and circular, approximately 7.8 mm in diameter. The stylomastoid foramen opens ventrally at the point medial to the mastoid process. The hyoid fossa opens at the posterolateral end of the tympanic bulla and it is 7.5 mm long and 5.0 mm wide. Slightly medial to the hyoid fossa, the carotid canal opens as size is 6.7 mm long and 4.9 mm wide. The anterior opening of the carotid canal is circular, moderate (4.5 mm diameter) and located at the anteromedial margin of the tympanic bulla.
The middle ear region of a long hexagonal petrosal is visible on the ventral floor of the braincase. Its anterior portion is positioned ventrally and is wider than its posterior portion. The petrosal crest is observed on the anterior part of the petrosal. A deep transverse sulcus lies on dorsal border of the petrosal, just below to the bony tentorium. The cerebellar fossa is dorsoventrally elliptical and has a small slit on the ventral part of the fossa. There is a knob-like tubercle on the medial margin of the cerebellar fossa. The internal acoustic meatus (internal auditory meatus) is anteroposteriorly elliptical, and the entrances for the cranial nerves VII and VIII are separated within the meatus.
The left side of the sphenoids are partially preserved, but the presphenoid and the dorsal half of the alisphenoid are missing. The ventral half of the alisphenoid forms the posterior wall of the choanal trough. The anterior opening of the alisphenoid canal is observed on the medial wall of the alisphenoid at the position of the orbital fissure. The posterior opening of the alisphenoid canal and the foramen ovale are joined in a common recess, and it is located just posterior to the laterally expanded pterygoid strut at the medial side of the mandibular fossa.
The pterygoid strut is dorsoventrally and transversely broad. There is a sharply edged ventromedial ridge present on the ventral surface of the pterygoid that extends from the posterior end of the palate to the long and slender, posteroventrally projected pterygoid hamulus.
The medial part of the palatal portion of the maxilla is broken away, but enough of that portion remains to show a transversely arched palate. The palatal margin of the maxilla is laterally divergent at the portion of M1. The infraorbital foramen is relatively small and dorsoventrally elliptical. The infraorbital canal runs through rather thick bone at the maxillary foramen. The dorsal roof of the infraorbital foramen is dorsoventrally thick. The orbit is large, however the medial wall of the orbit is broken away. On the ventral surface of the zygomatic root, there is a shallow fossa and a weakly developed ventral tuberosity.
The dorsal part of the premaxilla is not preserved. The rostral process is large and blunt. The palatine fissures (premaxilla foramina) are separated by a thin septum at the mid-portion, and each foramen is anteroposteriorly elongated (14.4 mm long and 5.6 wide on the right side).
The lateral half of the left palatine is preserved. The palatine is anteroposteriorly long, but its posterior borders with the pterygoid and the sphenoid are not clear.
The zygomatic arch of the jugal is long, thicker anteriorly and thinner posteriorly. Laterally, the zygomatic arch has a weakly curved and rounded orbital margin, a well-developed frontal process (postorbital process) on the dorsal margin, and a weakly curved masseteric margin ventrally. The outline of the anteroventral process is not clear because the maxilla-zygoma suture is closed. Posterior end of the temporal process projects dorsoventrally and rounded.
The mandibular symphysis is opened, rugose and is dorsoventrally long and elliptical. The posterior end of the mandibular symphysis is same level at the p2 alveoli. In dorsal and ventral view, the body of the mandible is slightly skewed laterally on its medial portion, just posterior to the m2 alveolus. The diastema between the canine and the first premolar is short. In lateral view, the dorsal and ventral borders of the mandibles are nearly parallel, but they diverge posterior to the coronoid process of the ascending ramus. The rami of the mandibles are V-shaped in dorsal view and curved posteriorly at m1. The anterior mental foramen is rounded, small (3.4 mm diameter) and located just beside the mandibular symphysis. The middle mental foramen is also circular, large (4.4 mm diameter) and located beneath p1. The posterior mental foramen is smaller (3.1 mm diameter) than both the anterior and middle mental foramina and located beneath p2. At the level of p2 and p3, a well-developed genial tuberosity is present on the ventral margin of the body. A narrow coronoid process is thinner dorsally, rounded and anterodorsally projected. A wide (39.2+ mm) and smooth condyloid process is present at the level of the tooth row. The mandibular notch opens wide anterodorsally. The angular process is weakly projected posteriorly and forms a small medial shelf. The masseteric fossa is shallow and its borders are unclear, with a weak horizontal crest at the dorsal part of the fossa. Medially, the mandibular foramen is small, dorsoventrally elliptical and directed anterodorsally. The mandibular canal, which is at the center of the broken surface of the right mandible, is also elliptical.
The dentition is represented by upper and lower alveoli on the left maxilla and both dentaries as I1-3, C, P1-4, M1-2, i2-3, c, p1-4 and m1-2. In addition, both I3s, right C and P2, and the lower canines are preserved in place. Isolated left I2 and P3, and the right P4 are also preserved.
The alveoli for I1 and I2 are transversely narrow but anteroposteriorly wide. The crown of the I2 consists of an anteriorly located large cusp and posteriorly located small cusplet. The I2 root is laterally thin and anteroposteriorly wide, and it is gently curved posteriorly. There is a distinct constriction between the crown and the root. A much larger isolated left I2 has a shallow groove on the lateral and proximal surface and is weakly curved posteriorly.
The strongly and anteriorly curved I3s have worn ends and are oval shape. The anterior surface of the crown is smooth, but the posterior surface makes a vertical crest.
The canine is not tusk-like, but large and conical, and it has a strong posterior crista. The root has a broken surface of the maxilla, which is very long and large (86.3 mm long in total of the canine), and transversely narrow. The proximal end of the root is visible from the broken cranium (see Fig 3A), and has an open pulp cavity.
The premolars are double rooted except for the P1. The P1 has a relatively large single root. The P2 has a narrow anterior and a wide posterior alveolus, and its crown has one small main cusp with a blunt lingual cingulum with several incipient cusplets. The P2 to M2 have narrow subcircular anterior alveoli and wide oval posterior alveoli.
Isolated left P3 and right P4, crowns have a posteromedially placed protocone shelf. They are similar in shape, but the P3 is slightly higher in crown height. The P3 has a posterolingual cingulum with one distinct cusp (protocone shelf) at the posteromedial margin of the cingulum. The P3 has a small cusp at the posterior end of the crown. The P4 has a more expanded protocone shelf and relatively large and high cusp also at the posterior end of the crown. It is anteroposteriorly slightly enlarged, forming a small blade-like ridge that is separated from the main cusp by a distinct notch.
The M1 is double rooted, and the posterior alveolus lies outside the general alignment of the cheek teeth. The alveoli of i2 and i3 are mediolaterally thin, anteroposteriorly long, and they are single rooted. The i2 alveolus is smaller than i3.
The lower canine is nearly equal size, but slightly shorter dorsoventrally and narrower transversely than the upper canine, and has a well developed posterior crista. Its root is almost oval with a weak longitudinal groove on the buccal side in cross section and is oriented dorsally.
The p2—m1 are double rooted, while p1 and m2 are single rooted. The p1 to p3 have bulbous crowns with well-developed enamel. An isolated left p3 is preserved, and possesses three distinct cusps; an anteriorly located developed cusp (paraconid), a main cusp (protoconid), and a small but distinct posterior cusp just behind the main cusp. The anterior cusp is smaller than the posterior cusp. The lingual cingulum is well developed and its surface is slightly crenulated. Its root is wider than the crown. The tooth row is short (63.6 mm).
The basihyoid, the left thyrohyoid and the ceratohyoids are preserved (Fig 8). The basihyoid is thickened toward both the proximal and distal extremities It has two small joints on the posterior margin for the thyrohyoid The thyrohyoid is missing part of the distal extremity, but its proximal extremity is thickened. The ceratohyoid is slender and it is thickened toward both the proximal and distal extremities. The proximal extremity of the ceratohyoid is about twice as wide as the distal extremity, and it has a flat edge and a nearly perpendicular articulation.
The wing process is large and extends ventrolaterally. The ventral tubercle of the ventral arch is weakly inflated ventrally. The lateral vertebral foramen is small and circular, and it is visible only in lateral view. The transverse foramen is also small; it is anteriorly circular and posteriorly triangular. The atlantal fossae are relatively weak, forming depressions ventral to the base of the wing. Each intraosseous canal opens posteriorly into the anterior transverse foramen. The transverse foramen is relatively large, and the odontoid fovea is also large and deep. Two shallow grooves extend transversely on the posterior surface of the ventral arch. A small and deep foramen is present on the mid-line of the posterior articular surface.
The axis is nearly complete, missing parts of the right anterior articular surface and anterior spinous process. The dens is large and thick. The blade-like spinous process extends posterodorsally. The dorsal margin of the spinous process is straight and anteroposteriorly long. The posterior edge of the spinous process expands laterally. The vertebral foramen is large and elliptical. The transverse process is large, and it is projected posterolaterally and ventrally. The transverse foramen is large and circular, and they are located at the base of the transverse process. On the ventral surface of the vertebral body, a pair of deep fossae are divided by a median crest. The anterior end of the median crest is developed as an anteriorly angled triangular tubercle.
Third to seventh cervical vertebrae.
The third to seventh cervical vertebrae are preserved (Fig 10D–10H). The transverse processes are long and knob-like in the third cervical, transversely thin and plate-like in the forth to sixth cervicals, and very weak knob-like in the seventh cervical vertebra. The spinous processes are projected weakly in the third to sixth cervical and strongly ventrally in the seventh cervical vertebra.
Seven thoracic vertebrae are preserved although their exact positions are not clear (Fig 10I–10O). The transverse processes are strongly projected in the “third, fifth to seventh” thoracics; squire shaped costal fovea are present on the transverse process. The spinous processes are projected posteroventrally in the “fourth and fifth” thoracics, but other thoracics are not well preserved.
Seven ribs are preserved. The left first to third ribs are nearly complete, but other ribs are preserved only proximal parts. The first rib is the shortest. The head and tubercle are distinct and well separated in each rib. Each rib is gently curved. The body of each rib is somewhat square in cross section, and therefore the anterior and posterior surfaces are relatively flat. The costochondral junction is semicircular and elliptical in cross section.
Two intermediary sternebrae are preserved. The sternebrae are short and thick, forming a square pole. Lateral thickness is wider than dorsoventral. It is thickened toward the anterior and posterior extremity. Both extremities are display a rugose articulation.
Both scapulae are well preserved (Fig 10A and 10C); the right scapula is nearly complete, missing only a part of the posterior angle, lateral margin of the spine, and the acromion. The dorsal part of the spine is thick and high compared to its ventral part. The base of the acromion extends ventral to the scapular notch. The scapular spine is positioned posteriorly; so that the supraspinous fossa is wider than the infraspinous fossa. Within the supraspinous fossa are two weak ridges parallel to the spine; the anterior one is weakly curved anteriorly, and posterior one is nearly straight. The scapular notch is deep. The anterior border is gradually curved. The posterior border is nearly straight. The scapular tuberosity is large. On the medial surface of the scapula, four muscule attachment ridges are present. Two most posterior lines are merged ventrally, forming a Y-shape.
The right humerus (Fig 10B) is nearly complete, but missing part of the ventral margin of the lateral epicondyle. The head is transversely small and anteroposteriorly long and elliptical. The greatest length of the head is around 20% of the total length of the humerus. An epiphyseal suture is still persistent at the anterior border of the head. The neck of the humeral head is indistinct. The shaft is relatively straight and slender. The greater tubercle is robust and elevated slightly above the head, and its dorsal surface is rugose. An elliptically shaped surface is present at the apex of the greater tubercle. The lesser tubercle is medially projected and located distinctly below the head. The intertubercular groove is narrow and deep between the greater and lesser tubercles. The tricipital line is present. The deltoid tuberosity is well developed on the pectoral crest. The pectoral crest is straight and directed distally toward the medial lip of the trochlea. The brachial groove is deep. The lateral epicondyle is conspicuously reduced and scarcely projected from the lateral margin of the distal radial capitulum. There is a deep groove on the lateral surface of the lateral epicondyle. The supinator ridge is weak and blunt. The medial epicondyle is knob-like and quadrangular in outline. The epicondylar foramen is absent. The capitulum of the humerus is low proximodistally. The trochlea is mediolaterally short. Both the olecranon and radial fossae are shallow. The supratrochlear foramen is absent. Although the distal tip of the trochlea and the posterodistal part of the capitulum are somewhat broken, the former is much greater in anteroposterior diameter than the latter as inferred from its width.
Relationships of the new fossil to other odobenids
The new fossil belongs to the Family Odobenidae in having a laterally expanded pterygoid strut (Character 13), a bony tentorium that is closely appressed to the petrosal (Character 29) and well-developed P1 and P2 with lingual cingula (Character 71). Those characters are recognized as unequivocal synapomorphies for the family [11–13]. Thus, the phylogenetic analysis for the new fossil was focused on members of the Odobenidae with member of other pinniped clades as outgroups. Previously Deméré  and Kohno [11, 12] presented cladistic analyses for the family Odobenidae mainly on the basis of cranial, mandibular and dental morphologies. Recently, Boessenecker and Churchill  analyzed additional characters of both crania and mandibles with cheek teeth of the odobenids. Although most of these characters were same characters used by Deméré , Kohno [11, 12], Kohno et al. , and Deméré and Berta , they defined all the characters used in their analyses more clearly and thoroughly illustrated on Morphobank (http://morphobank.org/index.php/Projects/ProjectOverview/project_id/530). Accordingly our data matrix is the one by Boessenecker and Churchill  with minor changes and an additional axial character (Character 91) for our analysis (S2–S5 Files). We included 17 odobenids and eight outgroup taxa that were used by Deméré , Kohno [11, 12], and Boessenecker and Churchill , and we also added extinct and early diverging arctoid, Potamotherium valletoni Geoffroy, 1833 (following Rybczynski et al. ) as an outgroup in this analysis. Among the taxa within Odobenidae, Pelagiarctos thomasi Barnes, 1988 and an indeterminate species belonging in the same genus reported by Boessenecker and Churchill  from the middle Miocene of California were excluded from our analysis because of the lack of any cranial material for this taxon at present. In total, our analysis used 17 ingroup and nine outgroup taxa coded for 91 morphological and morphometric characters (S2–S5 Files). Both character and tree data were manipulated using Mesquite 2.75 . A cladistic analysis was performed with TNT, 1.1 . All characters were unweighted and unordered. A heuristic search of 10,000 replicates was conducted, using tree bisection reconnection (TBR) and saving 10 trees per replication. To measure node stability, we calculated a bootstrap value using symmetric resampling with 2000 replicates and the decay index  for the strict consensus tree.
Our analysis resulted in 63 most parsimonious trees with 280 steps. The variations among the 63 trees are represented by differences in branching patterns among outgroup taxa and also ingroup taxa (mostly “dusignathines”) within the later diverging odobenids (see a strict consensus tree in Fig 12). Phylogenetic analysis revealed that the new fossil is recognized as an independent linage. The new fossil is distinguished from such earlier diverging odobenids as Prototaria spp, Proneotherium repenningi, Kamtschatarctos sinelnikovae, Neotherium mirum and Pseudotaria muramotoi in having two unequivocal and equivocal synapomorphies with later diverging odobenids such as the pentagonal basioccipital (Character 30) and straight dorsal margin of the spinous process of the axis (Character 91) respectively. However, the new fossil lacks synapomorphies of later diverging odobenids (i.e., Imagotaria downsi, Pontolis magnus, the “dusignathines” and the Odobeninae) such as the presence of ventral tuberosity of the zygomatic root of the maxilla (Character 7), shallow glenoid fossa (Character 26), large mastoid process of the squamosal (Character 33), absence of the metaconid on the lower cheek teeth (Character 70) and double rooted upper P3 roots (Character 74). Although not included within the computer-based phylogenetic analyses, Pelagiarctos thomasi and P. sp. of Boessenecker and Churchill  are clearly distinguishable from the new fossil by their very large size and robustness and by having extremely large cheek teeth. Therefore, the new fossil is differentiated from all previously known taxa within the Odobenidae. In addition, the new fossil has autapomorphic characters such as sharply divergent mandibular arch (Character 44) and slightly concave talonid basin of the lower cheek teeth (Character 69).
These distinctive features of the new fossil among taxa within the Odobenidae indicate that this taxon is monophyletic (Fig 12). Therefore, the generic level assignment as a new taxon is warranted for the new fossil described here. Thus, we propose Archaeodobenus akamatsui as a new genus and new species within the family Odobenidae.
Disparity of Archaeodobenus akamatsui and Pseudotaria muramotoi
Archaeodobenus akamatsui gen. et sp. nov. is presently known only from the holotype, which is from the top of the Ichibangawa Formation as described above. The same formation has also produced another odobenid Pseudotaria muramotoi Kohno, 2006. Therefore, both species are sympatric at least geochronologically. These two species of fossil odobenids are closely related to each other based on the phylogenetic analysis, but are not monophyletic. Indeed, the basioccipital in A. akamatsui is pentagonal in shape as a derived condition of all the later diverging odobenids, but the same portion in P. muramotoi is primitively parallel sided as in earlier diverging odobenids as well as the late Oligocene and early Miocene pinnipedimorphs. In addition, the mastoid process is small in A. akamatsui among the Odobenidae, but is stronger in comparison with the sister P. muramotoi. Also, the preserved cervicals in this new taxon show morphological differences between them (Fig 9). For example, the blade-like dorsal margin of the spinous process of the axis (Character 91) in A. akamatsui is recognized as a derived condition that unites this taxon with later diverging odobenids such as the modern walrus, Odobenus rosmarus and the Pliocene extinct walrus, Valenictus chulavistensis (SDSNH 36786: San Diego Natural History Museum) of the subfamily Odobeninae as the potential synapomorphy for all the later diverging odobenids such as Imagotaria, Pontolis and “dusignathines” as well as the monophyletic odobenines.
Our analysis also indicates that P. muramotoi does not have its own character (autapomorphy) and therefore the least modified condition in the transformation series of characters to the later diversing odobenids as suggested also by Kohno . In this sense, these differences between the two taxa within the same family in the same geologic age and same geographic range suggest that A. akamatsui might have split from P. muramotoi as a different species, with the rapid structural divergences during a short time period in the late Miocene in the western North Pacific.
Isolation and speciation of Archaeodobenus akamatsui and Pseudotaria muramotoi
The two different genera and species of the above mentioned fossil walruses from the same formation in a restricted geographical area suggests rapid diversification of later diverging odobenids, among the early late Miocene (between 10.0 and 9.5 Ma) around the Western North Pacific realm. In such case, knowledge of the depositional sequences of the sedimentary basin may be important to recognize cause of rapid diversification in marine mammals (e.g., Pyenson et al. ).
The depositional sequences at the locality area was studied by Takano et al, . According to them, the sea-level during the early late Miocene of the locality area had changed dramatically. In the beginning of the early late Miocene (12.5–10.5 Ma), the sea-level was receding, and the shelf structures at the locality had developed (Sequence 3, high stand phase). In addition, development of the fan delta system is known at this sequence. The sea-level during Sequence 4 (from 10.5 Ma) was receding then sudden transgression was initiated around 10.0–9.5 Ma. This sea-level rise is simultaneous with the condensed glauconite layer, from which both A. akamatsui and P. muramotoi were found. An association between glauconite and sea-level transgression has been previously reported [22, 23].
Considering the relationships between the sea-level changes and the diversification of the archaic odobenids, the occurrence of a regression phase just before the transgression may have been a driving force for the odobenid speciation during the late Miocene (see Fig 13). Firstly, during the transgression of Sequence 3, a common ancestor of both Pseudotaria muramotoi and Archaeodobenus akamatsui might have occupied a wide range along the western North Pacific coast, tied to availability of shoreline habitat for reproduction. Then, from the end of Sequence 3 to the beginning of Sequence 4 (11.0–10.0 Ma), the sudden sea-level fall resulted in reproductive isolation driven by considerable loss of their shelf habitats.
In contrast, Valenzuela-Toro et al  proposed that large-scale marine transgression was linked to local phocid extinction in the late Pliocene of Chile. Changing size of pinniped habitats and degree of sea-level can be considered with the chronological changes of the topography in different areas. The A. akamatsui locality was situated in shallow marine and close to the margin of the basin sloop . The land area decreased during the transgression stage, which could provide shallow shelf and suitable feeding habitat for the fossil odobenids. The area studied by Valenzuela-Toro et al  had large scale transgression, which resulted in much deep water, which were not suitable for the habitat of the pinnipeds.
There may be other explanation for odobenid rapid speciation and diversification during the early late Miocene. Based on the last record of contemporaneous desmatophocid pinnipeds from the early late Miocene Montesano Formation , these enigmatic pinnipeds might have reduced in population size and became extinct in the North Pacific  in the same period of the possible divergence time of Pseudotaria and Archaeodobenus. The estimation of the rapid speciation and diversification of these odobenids during the same time period might have been the evidence of the exchange of niche between the two families in the North Pacific. This may also be plausible but is not corroborated by sufficient evidence at present.
Also, Suto et al.  has discussed correlations between seqcuences of ocean productivities and evolution of marine organisms during the Neogene and Pleistocene based on the abundances of Chaetoceros resting spores (diatoms). According to their results, one of the rich productivities was recognized as the Pacific Chaetoceros Explosion Event (PACE-1) in the Late Miocene (i.e., Messinian, ca. 8.5–6.4 Ma), and its incipient increase was also recognized around 10 Ma in the North Pacific. In this regard, Churchill et al.  pointed out the productivity and climate change during the Messinian to have strong influence on otariid diversification and range. Although the synchronicity between the increase/decrease of ocean productivities and the marine transgression/regression cycles have not been clear, this may also have related to the fragmentation of the ancestral population and concecutive speciation of A. akamatsui and P. muramotoi, and the subsequent increase of the ocean productivity that promoted increase of both populations of two walruses in the locality area.
Newly speciated odobenids diverged allopatrically and migrated or invaded into the”locality area” around 10.0–9.5 Ma during the transgression period. Expansion of their habitats during the transgression just after the regression period allowed the cross over of their existences in the restricted area.
The geographical fragmentation of odobenid population during the period just before the sedimentation of glauconitic layer might have resulted in speciation of the Archaeodobenus-like odobenids from common ancestors with the Pseudotaria-like odobenids and subsequent increase in size of each population, which may resulted in the diversification of two separate species in the same locality area during the period between 10.0 and 9.5 Ma.
Pseudotaria and Archaeodobenus among the odobenids can, therefore, be recognized as the beginning of diversification among middle/late Miocene later diverging odobenids that are the two subfamilies Odobeninae+Dusignathinae+Imagotaria+Pontolis. As discussed above, the driving force of their speciation can be thought as is controlled by the rapid regression, which pushed both geographical and reproductive isolation. The two fossil odobenids from the same formation might show such case of the causal relationship between the sea-level fall and geographical isolation or segmentation.
Enigmatic odobenid Pelagiarctos
We did not include Pelagiarctos thomasi from the middle Miocene of California in our phylogenetic analysis because of the lack of its cranial material, but this enigmatic species might have been a member of the “later diverging odobenids” as has suggested by Boessenecker and Churchill . According to them, Pelagiarctos shares such derived characters as lateral lower incisors greater in size than medial ones (Character 54) and bulbous postcanine crowns (Character 63) with later diverging odobenids. However, these tooth characters are recognized not only in the odobenids but also in other pinnipeds such as allodesmine desmatophocids [29–31]. On the contrary, Pelagiarctos has distinctively double rooted cheek teeth like earlier diverging pinnipeds in spite of having aforementioned derived characters. In this regard, those derived characters may be altered as homoplastic when the cranial material for all the species can be included in the phylogenetic analysis. Therefore, we prefer to reserve judgment temporarily on the phylogenetic position of this enigmatic taxon based only upon the cheek tooth morphologies until the taxon is better understood by cranial material.
Archaeodobenus akamatsui gen. et sp. nov. represents the second taxon of the archaic odobenids from the early late Miocene (ca. 10.0–9.5 Ma) Ichibangawa Formation, Hokkaido, northern Japan. The same formation has also produced the archaic odobenid Pseudotaria muramotoi Kohno, 2006. These two odobenids are distinguishable from another in size and shape of the occipital condyle, foramen magnum and mastoid process of the cranium, and some postcranial features. Phylogenetic analysis reveals that A. akamatsui has two synapomorphies that unites the new species with later diverging odobenids (i.e., Imagotaria downsi, Pontolis magnus, the “dusignathines” and the Odobeninae). Therefore, two closely similar odobenids having relatively ancestral characters (P. muramotoi) and relatively derived characters (A. akamatsui) both lived in the same area during the same age. Perhaps the coexistence of two morphologically similar archaic odobenids as represented by A. akamatsui and P. muramotoi in the early late Miocene suggest their rapid speciations by geographical and reproductive isolation during a regressive phase and subsequent transgressions.
S1 File. Data of the body estimation of Archaeodobenus akamatsui.
S2 File. Specimen list.
S3 File. Character list.
S4 File. Data matrix in nexus format.
S5 File. Data matrix in TNT format.
We are grateful to Dr. Morio Akamatsu (formerly Historical Museum of Hokkaido, now Hokkaido Museum) for his encouragement and assistance throughout this study. Our thanks also go to the staff of the Tobetsu Town Board of Education who collected and deposited the holotype specimen of the new odobenid described here to the Hokkaido University Museum. We thank Yoshitsugu Kobayashi (Hokkaido University Museum) who received the specimen into the university museum collection and permitted us to study it. We are grateful to Yoshinori Hikida (Nakagawa Museum of Natural History) and Yuji Soeda (Hokkaido Museum) for their continuous assistance during our fieldwork and organization of the specimen deposition. The huge block of the nodule that contained the odobenid fossil described here was skillfully cut off and reduced by Shotaro Fujita, Satoru Itaya and Shigejiro Kanazawa (all Tobetsu Town), and the specimen was further prepared by Takako Furuya, Michiyo Ida, Sadakazu Kihara, Yoshiko Maguchi, Kousuke Nishikawa and Jun-ichi Nukazuka (then Chiba University) which are greatly acknowledged. We are also grateful to David J. Bohaska (United States National Museum of Natural History, Smithsonian Institution), Tomas A. Deméré (SDSNH), Tadasu Yamada and Yuko Tajima (National Museum of Nature and Science), Hitoshi Furusawa (Sapporo Museum Activity Center), and Sinji Isaji (Natural History Museum and Institute, Chiba,) for their permissions to examine comparative specimens. We are deeply indebted to Morgan Churchill (University of Wyoming) and an anonymous reviewer for constructive comments, and R. Ewan Fordyce and Robert W. Boessenecker (both University of Otago) for their pre-submission review. Morgan Churchill also helped to estimate the body size the new species. We are also indebted to Chieko Shimada (then Hokkaido University, now Akita University), Yoshihiro Tanimura (National Museum of Nature and Science) and Yukio Yanagisawa (Geological Survey of Japan) who have been generously shared for many years their extensive knowledge of collecting biostratigraphic information of the locality area. Finally, the senior author would like to express his deep appreciation to Yoshitsugu Kobayashi (HUM) and Hiroshi Nishi (Tohoku University Museum) for their encouragement and advice during the course of this research.
Conceived and designed the experiments: YT NK. Performed the experiments: YT NK. Analyzed the data: YT NK. Contributed reagents/materials/analysis tools: NK YT. Wrote the paper: YT NK.
- 1. The Kabato Collaborative Research Group (1995) Neogene stratigraphy of the Aoyama area, Tobetsu Town in the southern part of the Kabato Mountains, Hokkaido, Japan. Earth Science (Chikyu Kagaku) 49: 363–378.
- 2. Kakimi T, Uemura T (1958) Explanatory text of the geological map of Japan. Tsukigata 1:50000. Geol Surv Jpn Cruise Rep: 1–54.
- 3. Takano O, Hoyanagi K, Noto M, Ota K, Yahata M, Sedimentary facies group of the Kabato Collaborative Research Group (1995) Slope, shelf, fan delta and gravelly fluvial systems of the Neogene System in the southern part of the Kabato Mountains, Hokkaido, Japan. Earth Science (Chikyu Kagaku) 49: 253–270.
- 4. Takano O, Hoyanagi K, Noto M, Ota K, Yahata M, Sedimentary facies group of the Kabato Collaborative Research Group (1996) Formation processes of depositional sequences of the Neogene system in the southern part of the Kabato Mountains, Hokkaido, Japan. Earth Science (Chikyu Kagaku) 50: 9–28.
- 5. Yanagisawa Y, Akiba F (1998) Refined Neogene diatom biostratigraphy for the northwest Pacific around Japan, with an introduction of code numbers for selected diatom biohorizons. Journal of Geological Society of Japan: 395–414. doi: 10.5575/geosoc.104.395
- 6. Tsuji T, Saito Y, Ikuji Y, Ichinoseki T, Obuse A, Kai K (1992) Sedimentary environments and sequences of the Ponsubetsu and Subetsu Formations of the Minenobu Gas Field, northern Ishikari plain, central Hokkaido. Research Reports of the Japan Petroleum Exploration Research Center: 1–26.
- 7. Mead JG, Fordyce RE (2009) The therian skull: a lexicon with emphasis on the odontocetes. Smithson Contrib Zool 627: 1–248. doi: 10.5479/si.00810282.627
- 8. Sivertsen E (1954) A survey of the eared seals (family Otariidae) with remarks on the Antarctic seals collected by M/K "Norvegia" in 1928–1929. Norske Vidensk-Akad Oslo (Sci Res Norweg Antarct Exped 1927–1928 No. 36: 1–76.
- 9. Jefferson TA, Webber MA, Pitman RL (2008) Marine mammals of the world: a comprehensive guide to their identification. Oxford, UK: Academic Press.
- 10. Churchill M, Clementz MT, Kohno N (2014) Predictive equations for the estimation of body size in seals and sea lions (Carnivora: Pinnipedia). J Anat 225: 232–245. doi: 10.1111/joa.12199. pmid:24916814
- 11. Kohno N (1994) A new Miocene pinniped in the genus Prototaria (Carnivora: Odobenidae) from the Moniwa Formation, Miyagi, Japan. J Vertebr Paleontol 14: 414–426. doi: 10.1080/02724634.1994.10011568
- 12. Kohno N (2006) A new Miocene odobenid (Mammalia: Carnivora) from Hokkaido, Japan, and its implications for odobenid phylogeny. J Vertebr Paleontol 26: 411–421. doi: 10.1671/0272-4634(2006)26[411:anmomc]2.0.co;2
- 13. Boessenecker RW, Churchill M (2013) A reevaluation of the morphology, paleoecology, and phylogenetic relationships of the enigmatic walrus Pelagiarctos. PLoS ONE 8: e54311. doi: 10.1371/journal.pone.0054311. pmid:23342129
- 14. Deméré TA (1994) The family Odobenidae: a phylogenetic analysis of fossil and living taxa. Proc San Diego Soc Nat Hist 29: 99–123.
- 15. Kohno N, Barnes LG, Hirota K (1995) Miocene fossil pinnipeds of the genera Prototaria and Neotherium (Carnivora; Otariidae; Imagotariinae) in the North Pacific Ocean: evolution, relationships and distribution. Isl Arc 3: 285–308. doi: 10.1111/j.1440-1738.1994.tb00117.x
- 16. Deméré TA, Berta A (2001) A reevaluation of Proneotherium repenningi from the Miocene Astoria Formation of Oregon and its position as a basal odobenid (Pinnipedia: Mammalia). J Vertebr Paleontol 21: 279–310. doi: 10.1671/0272-4634(2001)021[0279:aroprf]2.0.co;2
- 17. Rybczynski N, Dawson MR, Tedford RH (2009) A semi-aquatic Arctic mammalian carnivore from the Miocene epoch and origin of Pinnipedia. Nature 458: 1021–1024. doi: 10.1038/nature07985. pmid:19396145
- 18. Maddison WP, Maddison DR (2011) Mesquite: a modular system for evolutionary analysis. Available at http://mesquiteproject.org.
- 19. Goloboff PA, Farris JS, Nixon KC (2008) TNT, a free program for phylogenetic analysis. Cladistics 24: 774–786. doi: 10.1111/j.1096-0031.2008.00217.x
- 20. Bremer K (1994) Branch support and tree stability. Cladistics 10: 295–304. doi: 10.1111/j.1096-0031.1994.tb00179.x
- 21. Pyenson ND, Irmis RB, Lipps JH, Barnes LG, Mitchell ED, McLeod SA (2009) Origin of a widespread marine bonebed deposited during the middle Miocene climatic optimum. Geology 37: 519–522. doi: 10.1130/g25509a.1
- 22. Huggett J, Gale A (1997) Petrology and palaeoenvironmental significance of glaucony in the Eocene succession at Whitecliff Bay, Hampshire Basin, UK. Journal of the Geological Society 154: 897–912. doi: 10.1144/gsjgs.154.5.0897
- 23. Obasi CC, Terry DO Jr, Myer GH, Grandstaff DE (2011) Glauconite composition and morphology, shocked quartz, and the origin of the Cretaceous (?) Main Fossiliferous Layer (MFL) in Southern New Jersey, USA. Journal of Sedimentary Research 81: 479–494. doi: 10.2110/jsr.2011.42
- 24. Valenzuela-Toro AM, Gutstein CS, Varas-Malca RM, Suarez ME, Pyenson ND (2013) Pinniped turnover in the South Pacific Ocean: new evidence from the Plio-Pleistocene of the Atacama Desert, Chile. J Vertebr Paleontol 33: 216–223. doi: 10.1080/02724634.2012.710282
- 25. Bigelow PK (1994) Occurrence of a squaloid shark (Chondrichthyes: Squaliformes) with the pinniped Allodesmus from the upper Miocene of Washington. J Paleontol 68: 680–684.
- 26. Kohno N (2005) Climatic change and the phylogenetic diversification with feeding adaptation of the pinnipeds. Fossil 77: 34–40.
- 27. Suto I, Kawamura K, Hagimoto S, Teraishi A, Tanaka Y (2012) Changes in upwelling mechanisms drove the evolution of marine organisms. Palaeogeography, Palaeoclimatology, Palaeoecology 339: 39–51. doi: 10.1016/j.palaeo.2012.04.014
- 28. Churchill M, Clementz MT, Kohno N (2015) Cope's rule and the evolution of body size in Pinnipedimorpha (Mammalia: Carnivora). Evolution: n/a-n/a. doi: 10.1111/evo.12560
- 29. Barnes LG, Hirota K (1995) Miocene pinnipeds of the otariid subfamily Allodesminae in the North Pacific Ocean: Systematics and Relationships. Isl Arc 3(4 for 1994): 329–360. doi: 10.1111/j.1440-1738.1994.tb00119.x
- 30. Kohno N (1996) Miocene pinniped Allodesmus (Mammalia: Carnivora); with special reference to the" Mito seal" from Ibaraki Prefecture, Central Japan. Transactions and proceedings of the Palaeontological Society of Japan New series: 388–404.
- 31. Deméré TA, Berta A (2002) The Miocene pinniped Desmatophoca oregonensis Condon, 1906 (Mammalia: Carnivora) from the Astoria Formation, Oregon. Later Cenozoic mammals of land and sea: tributes to the career of Clayton E Ray Smithsonian Contributions to Paleobiology 93: 113–147.