6 Fossiliferous sites and iodine sources

We will try to validate our model while seeking if the Hominids major part principal fossiliferous sites can be correlated, statistically, in space and time, with a volcanic and/or fissural local or close activity (located, in general, at a distance lower than 100 km and, to the maximum, in spite of the migrations dispersing factor, at a distance lower than 200 km). This proximity induces a probabilistic iodized food chain, favorable to the presence and the increase of the volume of the Hominids brain. We will not make distinction, in this study, between the various genera, species or subspecies (Ardipithecus ramidus, Australopithecus anamensis, afarensis... Homo habilis, rudolfensis, ergaster, erectus, sapiens, sapiens sapiens, etc...). We will take into account only the probable datings (because of the divergences according to sources, in M.Y.B.P. (Million Years Before Present), and the sites localization, until middle Paleolithic edge (approximately 0,09 M.Y.) or higher Pleistocene (approximately 0,140 M.Y.). The considerable demographic growth and migratory dispersions about this time, in all the world areas, then dilute the local probabilistic iodine influence. If, indeed, we take, at first approximation, like demographic parameter, the fossiliferous sites density criterion per a thousand of years, we note that in Cantabrie (Spain) for example, it goes from 0,03 sites in Acheulean to 8, 25 sites in Solutrean and 12 sites in Magdalenian is 400 times more (John Scarry 1998). Our search, without being exhaustive, counts, nevertheless, the principal known fossiliferous sites. The fossiliferous Neandertalians sites (and Preneandertalians) are a separate study subject as well as the Olduvai site.

In preliminary, we will examine the Aegyptopithecus and Dryopithecus cases; then fossiliferous sites by geographical areas.

Aegyptopithecus: Fayoum Primate, possible Dryopithecus ancestor, has an antiquated tail, cranial capacity: approximately 30 cc (Coppens 1992), Oman Sultanate. Fayoum lava layers of gone back to 24,7 +-0,4 and 27 +-2 (Simons 1985) - Yemen volcanic eruptions at the terminal Oligocene and the Miocene (Furon 1959); Aden Rift Gulf volcanicity from Miocene to current.

Dryopithecus (Proconsul): Three species (Ken Reeser 1998), Large monkeys and Man probable ancestor, cranial capacity 167 cc, does not have any more a tail, 22-18, sites in the Rusinga and Mfangano islands (Victoria Lake, Site 114 in volcanic ash) and in the North of Kenya (Walker, Teaford 1992) - Rift Valley volcanic miocene and pliocene zone.

Ternifine (0,650), Sidi-Abderrahman, Thomas, Sale (0,4-0,3), Rabat (0,3-0,175), Jebel Irhoud (0,12-0,08), Dar-es-Soltane, Temara, Mugharet El' Alya (0,06-0,035), Haua Fteah (0,08/0,04), (Gunter Brauer 1991) - Middle Atlas pleistocene volcanicity (north-western zone comparable in intensity with Puys d' Auvergne), of the Oujda area (Savornin 1931); only one site, recent, (Haua Fteah) is not near a proven volcanic zone. 10 sites.

Eastern Africa:

Aramis (Middle Awash 4,4-4,0), Addis-Abeba (2,5), Afar Valley (Hadar 3,4-3,0), Bodo (0,6), Dire-Dawa (0,07-0,04), Omo Valley (2,9-2,6-2,4-2,0-1,8-1,0), Omo Kibisch 1-2 (0,15-0,10), Omo Kibisch 3 (0,09-0,07), Allia Bay, Logatham, Kanapoi (East Turkana Lake 4,1-3,9-3,4-3,1), Koobi-Fora (East Turkana Lake 3,2-2,4-1,6-1,2), Ileret (East Turkana Lake 2,4-1,5-1,2-0,2-0,05), Turkana Lake (4,15-1,7), Nariokotome (West Turkana 1,9-1,6-1,2), West Turkana (2,6-2,5-2,4-1,8-1,7-1,0), Eliye Springs (0,18-0,12), Olduvai (1,85-1,7-1,6-1,4-1,15-0,8-0,6-0,4-0,015), Laetoli (3,8-3,5), Laetoli Ngaloba (0,15-0,12), Eyasi (0,25-0,18), Mumba-XXI (0,15-0,11), Bouri (2,5), Konso (1,4), (Hay 1976; Gunter Brauer 1991; Hay, Leakey 1992; Walker, Leakey 1992; De Bonis 1995; McBrearty 1996; Donald Johanson and Blake Edgar 1996; Ken Reeser 1998; Aaron Valenzuela, Mary Reed, Dr. Anna Pike-Tay 1999; Jim Foley 1999) - The large Rift Valley runs from Taurus to Beira on 6500 km. The african fault, the Rift Valley (Great Rift Valley and Gregory Rift Valley), is one of the terrestrial surface most spectacular characteristics. It extends, in Africa, of the Red Sea, in the Afar area (Ethiopia), until beyond the Zambezi river, on a distance of 4.000 km (Wallis 1936). On this almost distance totality, many volcanoes were active from Miocene to Current (Mac Connell 1972; Pallister 1979). Towards 8 M.Y., a Rift Valley volcanicity reactivation occurs. Towards 3 M.Y., the Rift Valley knows a volcanicity recrudescence (more than 120 eruptions during the last 2 million years in the Omo valley - Bardintzeff 1993) and the fissural eruptions (Furon 1968). All the Eastern Africa Hominids sites are under a volcanic near influence: Afar Triangle (Erta Ale); Omo Valley (Bardintzeff 1993); Kenya (Turkana Lake, Koobi Fora, Ileret: the Omo river arrival, pumice tuffs fossils extracted); Tanzania (Olduvai, Laetoli, Eyasi: Ngorongo, Oldoinyo Lengai, Kerimasi, Olmoti, Sadiman, Lemagrut etc...). 24 sites

Bahr el Ghazal area, close to Koro Toro (3,5-3) (Brunet 1995) - Fossil close to the Djourab erg, bathed at plio-pleistocene by wadis which went down from the Tibesti Massif whose volcanicity was very active at that time (Prichard 1979) and gave rise to a hydrographic network in all the area, currently reduced to dry valleys (Furon 1968). 1 site

South Africa: (White 1989; Günter Brauer 1991; McBrearty 1996; Keen Reeser 1998; Jim Foley 1999).

Broken Hill (0,25-0,2-0,18-0,125) - Volcanicity and quaternary fissural eruptions of the Rift Valley southernmost end, towards the Zambezi.

Taung (2,8-2,3-2,0-1,0), Makapansgat (2,8-2,3), Sterkfontain (2,8-2,5-2,3-2,0-1,9-1,5-1,2), Kromdraai, Swartkrans, Gladyswale (2,0-1,9-1,8-1,6-1,5-1,2) - Great Dyke (450 km of eruptive rocks and magmatic flows, plio-pleistocene faults with fissural eruptions) (Furon 1968).

Cave of Hearths (0,22-0,18), Border Cave (0,1-0,07), Florisbad (0,18-0,12-0,10) - Great Dyke (450 km of eruptive rocks and magmatic flows, plio-pleistocene faults with fissural eruptions) (Furon 1968).

Hopefield (0,4-0,25), Kelders Cave (0,08-0,06), Klasies River (0,12-0,08) - a volcanic influence is not proven for these 3 sites. 13 sites

Qafzeh (0,12-0,08), Skhul (0,12-0,06), Hayonim (0,08) (Hublin, Tillier 1991; McBrearty 1996; Patrick Quinney 1996), Ubeidiya (1,4) (Larrick and Ciochon 1996), Kebara Cave (0,06), Amud (0,07), Tabun (0,1) (Quinney 1996), Zuttiyeh (0,13) - these layers are concentrated on a surface lower than 50 km in diameter (Ofer Bar Yosef, Bernard Vandermeersch 1991); close volcanicity (approximately 50Km): Hasbani basalt (Hula Valley) 0,13 - 0,073 +-0,014, El Furn Flow 0,079 +-0,013, Alequa Flow 0,064 +-0,013 (Golan Plate), Raqquad Basalt (close to the Tiberiade Lake) 0,13 - 0,07, Golan basalt flow 1,8 to 1 (Horowitz 1979). If the mousterian population in Israel is very abundant, it seems that the superior Paleolithic human remainders are very rare there. In parallel, the superior Paleolithic did not know significant volcanicity. 8 sites

Shanidar I (0,1-0,04) (Ken Reeser 1998; Jim Foley 1999) - plio-pleistocene tectonic until the Current one with haulage then setback of still active Zagros with recent faults (Ricou, Braud, Brunn 1977). 1 site

Narmada Valley, Indus Valley (0,2?) - Indus depression fracture, plio-pleistocene ophiolites (Bassoullet, Colchen, Mouterde 1977). 1 site

Teshik-Tash (higher Pleistocene) - Pleistocene end tectonic activity with Hissar chains rising and dislocation, Pamir and the Hindu-Kouch (Davis, Ranov, Dodonov 1985). 1 site

Bisitun (higher Pleistocene) - Zagros chain plio-pleistocene tectonic (Ricou, Braud, Brunn 1977). 1 site

Dmanisi (South-western of Tbilissi) (1,8-2,0) mandible found immediately above a lava basaltic layer (Gabunia, Vekua 1995), 2 craniums (gone back to 1,75) resting on a lava layer (gone back to 1,85) (Gabunia 1999) - lower Pleistocene volcanicity in eastern Anatolia (Kars area) (Brinkmann 1976). 1 site

Riwat, Pabbi Hills (1,9) (Larrick and Ciochon 1996), Riwat Site 55 (0,045) - Indus depression fracture, plio-pleistocene ophiolites (Bassoullet, Colchen, Mouterde 1977). 2 sites

After a first volcanic cycle in middle Miocene, the Java island knows a second volcanic cycle at Neocene then third at Pleistocene. The Notopuro period (middle and superior Pleistocene) is, in particular, an intense volcanic activity theatre in the Solo Zone.

Sangiran 17 (1,7-0,8) (Jim Foley 1999), Sangiran (1,66) (Larrick and Ciochon 1996): central Java - lower and middle pleistocene volcanicity (volcanoes Sundoro, Sumbing, etc...); Sambungmachan (1), Ngandong (Solo river alluvia) (0,5-0,2): Eastern Java (volcanoes Merbabu, Merapi Lawu, Djobolarangan, etc...) - Solo Zone middle and higher Pleistocene volcanicity; Modjokerto (1,81) (Larrick and Ciochon 1996), Trinil (1,8), (Trinkaus, Shipman 1996), Trinil 2 (0,7) (Jim Foley 1999): Eastern Java - Eastern Solo Zone pleistocene volcanicity (volcanoes Andjasmoro, Kelud, Kawi, Welirang, Ardjuno, Butak, etc...) (Van Bemmelen 1970). 7 sites

We retained, as indicated more high, only the sites former to higher Pleistocene (approximately 0,140 M.Y.).

Yingkou, Jinniushan (0,20-0,10), Benxi, Miaohoushan, Locality A (0,20), (Liaoning); Yiyuan, Qizianshan (middle Pleistocene), (Shandong); Nanjing, Tangshan (0,40-0,20), (Jiangsu); Hexian, Longtandong (0,30), Chaoxian, Yenshan (0,20-0,25), (Anhui); Jiande, Wuguidong (0,15), (Zhejiang); Shaoguan, Maba, Shiziyan (0,20-0,10), (Guangdong) - eastern stages belt Yanshanian and Himalayan characterized by its volcanic activity, Tancheng-Lujiang earth's crust and deep faults fractures zone. Zhoukoudian, Locality 1 (0,50-0,30), (Beijing Municipality); Xanggao, Xujiayao (0,10), Xiangfen, Dingcun (0,10), (Shanxi); Nanzhao, Xiaohuashan (middle Pleistocene), Xichuan (middle Pleistocene), (Henan); Yunxian, Quyuan, River Mouth (0,65-0,55), Yunxian, Longgudong (middle Pleistocene), Yunxi, Bailongdong (middle Pleistocene), Jianshi, Longgudong (middle Pleistocene), Changyang, Wanlongdong (0,15), (Hubei): Xingan-Taihang earth's crust and deep faults fractures zone, Taihang mountains risings and quaternary cracks. Lantian, Gongwangling (1,15), Luonan, Donghecun (higher Pleistocene), Lantian, Chanjiawo (middle Pleistocene), Dali, Tianshuigou (0,18), (Shaanxi); Rifts valleys quaternary cracks. Wanxian, Wushan, Longgupo (1,9), (Sichuan); Tongzi, Yanhuidong (final middle Pleistocene), (Guizhou): no proven sources; Yuanmou, Danawu (lower Pleistocene), (Yunnan) - Bangong-Nujiang deep faults ? (Hublin 1992), Chinese Fossil Hominids (1996), (Zunyi, Yuqi, Hongzhen 1986). 25 sites  

The european fossiliferous sites enter within the neandertalians and preneandertalians sites framework.

If we examine the whole quoted world fossiliferous sites, we note that on these 95 indexed sites, 88 are under volcanic and/or fissural influence and 7 do not undergo, in a proven way, these influences: Haua-Fteah (0,08-0,04) in North Africa; Hopefield (0,4-0,25), Klasies River (0,12-0,08) and Kelders Cave (0,08-0,06) in South Africa; Wanxian, Wushan, Longgupo (1,9), Tongzi, Yanhuidong (final middle Pleistocene), Yuanmou, Danawu (0,90-0,50) in China. A correlation of 92,6 % (88/95), in space and time, between the fossiliferous sites and the volcanic and fissural zones close excludes any randomly distribution and consolidates our model.

Before analyzing the Olduvai site, let us evoke the Laetoli series (Richard Hay, Mary Leakey 1981). Located at a 20 kilometers score in the south Olduvai throat, it comprises volcanic rocks made up of wind tuffs (for the three quarters) and of air tuffs. One found, in this series, steps prints gone back from 3,8 to 3,5 M.Y. All the wind and air tuffs come from the Sadiman volcano located at 17 km in the east and gone back (K-A) to approximately 3,7 M.Y. Later, lava floods coming from the volcanoes Sandiman and Lemagrut and gone back to 2,39 +-0,09 M.Y. covered the old tuffs.

We will now analyze the fossiliferous Olduvai site (Richard L.Hay 1976).

The Olduvai throat is located on the Large African Rift Valley eastern branch western edge, in the Serengeti plain, in the north Tanzania. The Olduvai throat, since layer I to the Ndutu and Naisiusiu layers, knew, at Pleistocene, a primarily volcanic environment due to the volcanic rocks and the volcanoes located especially at the throat south and east. The volcanic products dominated the various fossiliferous sites environment either by the volcanoes sides sediments drainage or by fissural emissions or by the air or wind tuffs deposit, especially brought by the winds coming from the south, the east and north-east volcanoes,. The Olduvai throat various series examination confirms the fossiliferous sites temporal (in million years M.Y.) and spacial concomitance and a near volcanic activity.

The Olduvai throat fossiliferous sites comprises 7 formations:

Layer I: Sites from 1,85 to 1,70 (Australopithecus, Homo habilis - 20 known sites): Ngorongo eruptions tuffs and ashes (2,45 to 2), Olmoti eruptions tuffs and lava (1,85 to 1,65).

Layer III: Oldowaian developed and acheulean sites from 1,15 to 0,8 (Homo erectus): many volcanic refuses deposits, air tuffs especially brought by the winds coming from the east and the north-east volcanoes.

Layer IV: Oldowaian developed and acheulean sites from 0,8 to 0,6 (Homo erectus), 3 times more sites than in layer III: metamorphic and volcanic refuses deposits, air tuffs brought especially by the winds coming from the east and the north-east volcanoes.

83 sites known in layers III and IV.

Masek Layers: 1 known site, from 0,6 to 0,4 (Homo erectus): Volcanic ash emitted almost entirely by the Kerimasi volcano; Swallow Crater middle dating (K-A) 0,37.

Ndutu Layers: 2 sites known, one towards 0,06, the other towards 0,03 (Homo sapiens): deposits from 0,4 to 0,03; Oldoinyo Lengai principal ashes sources gone back from 0,06 to 0,015.

Naisiusiu Layers: 1 known site 0,017 (Homo sapiens): Oldoinyo Lengai wind tuffs gone back from 0,022 to 0,015.

It is remarkable to note the known fossiliferous sites very reduced number (4) of the Masek, Ndutu and Naisiusiu layers which were subject to the Kerimasi and Oldoinyo Lengai volcanoes volcanic influence activity located relatively far (approximately 55 km of the Olduvai throat) whereas the other layers (I, II, III and IV), with much more sites (212), were under the close volcanoes volcanic influence activity (a few km): Olmati, Ngorongo, Sadiman, Lemagrut.

All the layers are under volcanic influence (ashes, wind or air tuffs, sediments and refuses volcanic, etc...) and when the emissions are dated, they coincide with the fossiliferous datings: Laetoli: Sandiman; layer I: Ngorongo, Olmoti; Masek layers: Kerimasi; layers Ndutu and Naisiusiu: Oldoinyo Lengai.

Homo sapiens neanderthalensis or Homo neanderthalensis and its ante wurmian predecessors (Hublin 1998).

Many paleoanthropologists regard Homo heidelbergensis as the antiquated Homo sapiens common ancestor in Africa and Neandertalians in Europe. The researchers working at Gran Dolina (Spain) estimate that Homo antecessor (0,780 M.Y.) is the Homo sapiens and Homo heidelbergensis predecessor (Amelie A.Walker 1997). Other paleoanthropologists dispute the designation of Homo antecessor like a new species (Rightmire, Stringer, Hublin). Recent genetic studies suggest that the Neandertalians and human modern ancestors diverged towards 0,5 M.Y. One can consider the Mauer mandible (0,5 M.Y.) like pertaining to Homo heidelbergensis. He would be the Neandertalians and their antewurmian predecessors ancestor (Mark Rose 1997). Traditional Neandertalians are gone back from approximately 0,075 to 0,026 M.Y. (Zaraffaya, Patrick Kinney 1996), with some a little older (Biache, Saccopastore, La Chaise B-D layers). One can count, currently, more than 315 individuals remainders (Heim 1997). Their cerebral capacity middle value is 1518 cc + - 169 cc (Hublin, Tillier 1991). Trinkaus and Howells (1992) quote 106 Neandertalians sites (and their precursors) including 95 Europeans (35 are located in the Massif Central). Hublin and Tillier (1991) quote 84 European sites (of which 17 approximately are localised in the Massif Central).

In accordance with our probabilistic model, we will seek if the 84 fossiliferous neandertalians european sites major part, quoted by Hublin and Tillier, can be correlated, statistically, in space and time, to a volcanic and/or fissural activity local or close (located, in general, at a distance lower than 100 km and, to the maximum, in spite of the dispersing migrations factor, at a distance lower than 200 km). Note that the trachytic clouds can settle very far (eruptions from the Chaine des Puys whose finest products fell down in the Chalain Lake sediments , Jura, and Switzerland, that is to say to several hundred km - Kraft, de la Rouziere 1991).

I Sites under near volcanic influence (sources located from 0 to 100 km):

10 Cesaire Saint, 12 Monsempron, 13 Quina, 14 Le Petit Puymoyen, 15 La Chaise, 16 Le Placard, 17 Marillac, 18 La Cave, 19 Montgaudier, 20 Fontechevade, 21 Castaigne, 22 Roc de Marsal, 23 Le Moustier, 24 Regourdou, 25 Ferrassie, 26 Pech de l'Aze, 27 Combe Grenal, the 28 La Chapelle-aux-Saints, 46 Angles-sur-l' Anglin, 29 Vergisson, 51 Arcy-sur-Cure, 55 Genay - 22 sites: Massif Central plio-pleistocene volcanicity, largest volcanic mountain mass of Europe with that of Etna (Bardintzeff 1993); Chaine des Puys, volcanic activity from 18 M.Y. to 0,250, an eruptive cycle occurs from 0,090 to 0,003 with a maximum towards 0,010 (Puy de Chanat 0,090) (Brousse, Lefevre 1990, Bardintzeff 1993, Lorenz 1980); Petite Chaine des Puys and Chaine de la Sioule, Chaine des Puys synchronous cycle (Puy de Chalard 0,051) (Brousse, Lefevre 1990); Cezallier, miocene (8-5,4 M.Y.), pliocene (5,4-3 M.Y.) volcanicity and revivescence from 0,240 to 0,006 M.Y. (Brousse, Lefevre 1990); Mont-Dore mountain mass, volcanic activity from 5,5 to 0,25 (Lorenz 1980).

11 Montmaurin, 30 Malarnaud, 31 Le Portel, 32 Caune de l' Arago, 33 La Crouzade, 34 Hortus, 35 Macassargues, 36 Orgnac, 37 La Masque, 38 Bau de l' Aubesier, 39 Les Peyrards, 40 Rigabe, 41 Grotte Putride, 42 Pie Lombard, 43 Le Lazaret, 44 Le Prince - 16 sites: Deves, volcanicity from 2,7 to 0,59 (with broad fissural flows); Velay, miocene, pliocene, pleistocene volcanicity (Kraft, de la Rouziere 1991); Escandorgue, Agde, volcanicity from 2,5 to 0,7; Lodevois volcanicity (Ante-Riss and Riss) from 0,4 to 0,10 (Debrand-Passard 1984); Bas-Vivarais, volcanicity former to 0,035 (Ray-Pic flow) up to 0,011 (Lorenz 1980); Languedoc Province volcanicity from 3,3 to 0,7 (Lorenz 1980); Provence Ponto-Pliocene-Current volcanic district (La Garde) (Campredon, Boucarut 1975); Olot (Spain) volcanicity from 0,7 to 0,010 (Brousse, Lefevre 1990).

67 Fate, 68 Buca del Tasso, 69 Castel di Guido, 70 Grottoni di Calascio 71 Saccopastore, 72 Sedia del Diavolo, 73 Mont Circe, 83 Archi - 8 sites: western Italy coast bordered of quaternary volcanoes from Tuscany to Sicily (Furon 1959); volcanic provinces: 1) Tuscan province, Monte Amiata 2,3-0,185, Radicofani 0,43; 2) roman province, Vulsini Mounts, Bolsena Lake 0,43-0,13, Cimini Mounts, Vico Lake 1,2-0,095, Sabatini Mounts, Bracciano Lake 0,438-0,225, Albains Mounts, Albano Lake 0,706-0,0295; 3) campanian province, Rocccamonfina 0,46-current, Phlegreans Fields superior-current Pleistocene, Ischia inferior-current Pleistocene; 4) sicilian province, Eolian Islands 0,43-current, Etna 0,30-current, Lipari Islands 0,16-current, Stromboli 0,66-current (Kraft, de la Rouziere 1991).

84 Petralona - 1 site: Macedonia recent pleistocene volcanicity (Lorenz 1980).

50 Engis, 52 Biache, 53 Spy, 54 La Naulette, 56 Fond-de-Foret, 57 Neandertal, 58 Salzgitter-Lebenstedt, 59 Wildscheuer, 60 Mauer, 61 Steinheim, 63 Ehringsdorf, 64 Taubach - 12 sites: Eifel-West from -0,4 to -0,012 and Eifel-Laach from -0,57 to -0,011 volcanoes (the volcanic materials dispersion surfaces are often significant, being able to go to Berlin, the Constancy, Zurich, Geneva lakes, etc...) (Kraft, de la Rouziere 1991).

1 Columbeira, 2 Forbes Quarry, 3 Devil's Tower, 4 Zafarraya, 5 Cariguela, 7 Cova Negra, 8 Agut, 9 Banolas - 8 sites: Condeixa wurmians tuffs (western of Coimbra); powerful trachyandesite flows in Miocene being prolonged to the Plio-Quaternary in the betic Cordilleras (Auboin, Brousse, Lehman 1985); termination N.E. quaternary volcanic rocks of the Catalan Coastal Chains; volcanicity and pleistocene faults of the betic Cordilleras, Grenade depression quaternary faults, Alicante and Almeria faults, marked out by significant eruptive buildings (Cabo de Gata) (Lorenz 1980);

Total: 76 sites.

II Sites under possible volcanic influence (sources located at more than 100 km):

65 Zhaskhalnaya, 66 Kiik-Koba: Eastern Mediterranean plio-quaternary volcanicity, Dinarides, Balkans and Minor Asia (Auboin, Brousse, Lehman 1985) - Total: 2 sites.

III Sites without proven volcanic influence:

6 Atapercua, 47 La Cotte de Sainte Brelade, 48 Pontnewydd, 49 Swanscombe, 45 Cotencher, 62 Vergranne - Total: 6 sites.

On the 84 analyzed sites, one notes that 90 % (76/84) are under volcanic influence, 2 % (2/84) under possible volcanic influence and 8 % (6/84) without proven volcanic influence. If one uses the Erik Trinkaus and William Howells statistics (1992), with 35 sites located in the Massif Central (instead of 19 in the Hublin-Tillier statistics), under volcanic influence, one obtains the following percentages: 92 % (92/100), 2 % (2/100) and 6 % (6/100).These percentages establish an unambiguous correlation between the localization of the sites and a near volcanic influence excluding any randomly distribution from the fossiliferous sites.

The analysis that we have just made of the Hominids fossiliferous sites in the world, from the Pliocene beginning (approximately 5 M.Y.) to the superior Paleolithic beginning (0,035 M.Y.), if it is not exhaustive, is statistically significant because it counts sites known worlwide. This analysis results, of that of a precise site chronology layers, the Olduvai site converge: 92 % of the world sites (88/95), all the Olduvai layers (7 layers, 100 %), as well as the Laetoli series undergo the volcanic and/or fissural emissions influence more or less close. As for the fossiliferous neandertalians and preneandertalians european sites, 90 % (76/84) or 92 % (92/100), according to the authors statistics, are localised in the volcanic zones vicinity (0 to 100 km on middle).

One can note, that in Europe, the currently known oldest sites are located in Velay where the Hominids presence is certain around 1 M.Y., probable between 1 and 1,5 M.Y. and possible around 2 M.Y. In south-east France, the oldest sites have a probable age between 1.3 and 1 M.Y. (Besse-sur-Isole, Var, 1 M.Y.; Le Vallonnet, close to Menton, 0,9 M.Y.) (Debrand-Passard 1984). Let us point out the Chilhac peeble tools gone back to approximately 1,5 M.Y. Tardily , quote Orgnac III (Ardeche), and Terra Amata in Nice (towards 0,6 M.Y.) These datings coincide with those of surrounding volcanicities: Velay (plio-pleistocene), Causses, Escandorgue, Low-Languedoc (plio-quaternary), Deves (2,7-0,59 M.Y.), Coirons (Miocene-Quaternary) (Kraft, de la Rouziere 1991), volcanic district of Provence Ponto-Pliocene-Current (La Garde) (Campredon, Boucarut 1975).

The statistical correlation established between the volcanic and/or fissural iodine sources and the fossiliferous sites validate our probabilistic interaction model between the iodine stimulus and the Hominids cranial capacity evolution (from 167 cc for Proconsul to approximately 1350 cc for Homo sapiens sapiens and 1450 cc for Homo sapiens neanderthalensis).

One observes, a contrario, the fossiliferous Hominids sites almost total absence, until about the towards middle Paleolithic end, in the areas deprived of volcanic activity at plio-pleistocene. Let us exclude America and Australia whose settlement would go up about towards the middle Paleolithic end. In Europe, particularly subjected to the quaternary glaciations, intersected with interglacial, one notes the about complete Hominids absence, in the western areas, except for some rare sites in Great Britain (Pontnewydd, Swanscombe), from the Pyrenees to the Baltic States, at the Atlantic edge, at Channel, at the North Sea and Baltic (Brittany, Normandy, Belgium, Netherlands, germano-polish, baltic, russian plains), Bielorussia, ukrainian plain. In Africa, outside North Africa, Eastern and South Africa, and north Chad activity, the whole of all the west african, which does not express a significant volcanic activity, does not seem to contain fossiliferous Hominids sites. In Asia, the principal fossiliferous sites are in Java (primarily volcanic island), in China, in volcanicity and fractures zones and, to a small extent, in the Narmada Valley, in India, in the Indus fracture hollow zone. Most of North Asia, inhospitable, does not conceal Hominids remainders (Siberia plains and central Siberia plate, subjected to the quaternary glaciations). The indian sub-continent, hospital, but without notable plio-pleistocene volcanic activity, does not contain fossiliferous layers (except for the hollow Indus).

At the inferior Paleolithic end (towards 0,12-0,13 M.Y)., Homo sapiens appears, probably in Eastern Africa (Kenya, Tanzania), migrates to the Middle East, to South Africa, to Europe, to Central Asia then towards the New-World (Donald Johanson and Blake Edgar 1999). The Homo sapiens origin, african or regional, the sharp controversies object remains.

In France, the civilizations which follow one another at the superior Paleolithic refer all, more or less, to the Massif Central volcanic area : Chatelperronian (close to the Chaine des Puys; 37-35 / 30 b.c.), Aurignacian (Massif Central Southern; 33-30 / 27-25 b.c.), Gravettian (Chaine des Puys-Cezallier; 27-25 / 20-18 b.c.), Solutrean (Chaine de la Sioule; 20-18 / 15 b.c.) and Magdalenian (Massif Central Southern; 18-15 / 10-9 b.c.) (Hours 1987; Camps 1994; Lorblanchet 1999). The french prehistoric sites concentration is particularly intense in the Massif Central with the superior Paleolithic like were the fossiliferous sites with the middle Paleolithic: Dordogne and Vezere valleys, its affluent, resulting from the Millevaches Plate to the Chaine des Puys foot whose volcanicity knows its apogee towards 0,010 B.P. (Bardintzeff 1993). The superior Paleolithic end sees the ground climate approaching that current and the fundamental transformation of the conditions of live of the populations, which pass from the hunter-collectors stage to that of farmer-breeders, accompanied of a considerable demographic growth. As we have recalled it at the beginning of this chapter, if we take, at first approximation, like demographic parameter, the fossiliferous sites density criterion per a thousand of years, we note that in Cantabrie (Spain) for example, it goes from 0,03 sites in Acheulean to 0,21 sites at the Chatelperronian beginning and to 12 sites at the Magdalenian end, that is to say 57 times more, in approximately 25.000 years, from the beginning to the end superior Paleolithic (John Scarry 1998). Then the " Neolithic revolution " occurs. The urbanization modifies the social relations, the cultures and the populations densities which are spread through the ecumene (Catal Huyuk 6500-5600 b.c., with an estimated population at 5000/7000 people) (Camps 1994).

During last five millenia, the Neolithic era gives rise to five historical civilizations principal hearths (regarded as the greatest societal units, Toynbee 1934-1961), more or less correlated with volcanic areas, and which will be at the ecumene current settlement origin (Breton 1991): 1) The Mediterranean-Middle-East (Mesopotamie, Nile Valley, Crete; 3rd millenium b.c.) - Zagros and Aegean Sea recent faults, Miocene/Current Cyclades archipelago volcanicity: Aegina Gulf, Milos, Santorin, etc... (Kraft, de la Rouziere 1991); 2) India (Indus Valley, Harappa, Mohenjodaro; 3rd millenium b.c.) - Indus hollow fracture (Bassoullet, Colchen, Mouterde 1977); 3) China (2nd millenium b.c. yellow and blue rivers basins) Tancheng-Lujiang and Xingan-Taihang earth's crust fractures zone and quaternary major faults, Taihang mountains risings and quaternary cracks (Zunyi, Yuqi, Hongzhen 1986); 4) Mexico (olmeque civilization, 2nd millenium b.c.; Tabasco, Veracruz in the Gulf of Mexico) - volcanic Top-Plates; 5) Peru (Chavin civilization; 1st millenium b.c.) - Andes Cordilleras volcanic High-Grounds.

One can conclude, with much probability, that the Hominids evolution, since the Proconsul appearance, while passing by their divergence with Panids, approximately 7 M.Y. (Lewin 1996) ago, until the arrival of the Cro-Magnon type modern man, was carried out, for a dominating share, in the vicinity and under the influence of the volcanic iodine sources. Whereas at Pliocene and Pleistocene, the most signifiant iodine sources seem to be in the volcanic areas, the iodine diffusion during millions of years and its scrubbing at the ground surface will lead to the current situation where the iodine principal vectors, as mineral as biological, the seas and the oceans appear, then the lakes and the rivers, as it will be indicated in chapter 1 (The iodine sources), whereas the volcanic origin iodine see its influence if not disappear, at least stand apart, as we can it note in the chapter VIII. In addition, "the today volcanic eruptions are only rabbit farts, compared with the last enormous volcanic crises " (Brack, Raulin 1991).

Moreover, we propose a crucial test, likely to confirm or cancel, with the popperian direction (Popper 1980), our probabilistic relation model between the hominisation and the iodine sources. The analysis of the contents of the sedimentary rocks iodine, on the one hand with the geological times thread, on the other hand on the same stratigraphic level between the significant fossiliferous Hominids sites and the sedimentary rocks free from Hominids fossils appears likely to us to be able to confirm or cancel, in a statistical way, the credibility of our assumption. It is what we tried to do, in the following chapter, while analyzing, quantitatively, Homo sapiens sapiens settlement densities, today, on our sphere surface, in correlation with its environment iodine contents.