Global Warming and Earthquakes.

We’ve often heard it said that warmists will link any disaster with global warming with earthquakes being the quintessential disaster that has no connection with the weather. But personally, I’m not sure that we should be so dismissive. Although what follows is pure speculation. It has about the same scientific basis as: “CO2 must cause warming”, in that it may be very simplistic simply lacks empirical evidence to support it but it is worth more investigation.

The Theory

If the surface of the earth warms, then, we’d expect that warming to penetrate beneath the surface of the earth and for the earth’s crust to warm as well. We can calculate how fast this might happen based on basic principle. Rock has a thermal conductivity of about 5 W/m.K (range is 2-7). Basalt rock has a heat capacity of 0.84 Kj/KG K and a density of 3011 kg/m3. If we assume a 10km thick crust and a 1C rise in temperature spread evenly through the crust, the heat conduction through this is:

5 x10-4 W/m2.

How long would this heat flow take to heat the crust? The weight of 10km of basalt is:

3011 x 10,000 = 3.011 x 107 KG/m2

Heat capacity per square meter of 10km of basalt rock is therefore

3.011 x 107 x 840 j/K = 2.5 x 1010

So a rough estimate for this mass of rock to heat by an average of 0.5C (1C at surface dropping to 0C change at 10km) with a typical value of heat conduction is :

(2.5 x 1010 j/K x 0.5K)/5 x10-4 W/m2. =2.5 x 1013 seconds. = 800,000 yrs

Whilst this is a very rough and ready calculation of the heating and falsely assumes a linear heat profile, it’s near enough for our purposes to show if there is an appreciable affect. But, even given the hand waving argument, there’s no way that a century of global warming is going to significantly warm the crust. But what about a much longer period change, like the last iceage. An iceage tyically has around 10C variation in temperature. That increased temperature difference brings down the time to see appreciable warming (an average 0.5C change) to perhaps 80,000 years  and this is very comparible with the time between ice ages as there have been 4 in the last 400,000 years.

The Creaking earth

As everyone knows, warming causes expansion, so how much will the earth’s crust warm for a 0.5C change in crustal temperature? Expansion coefficient of basalt is about 5×10-6 per degree change. So the expansion of the crust at the equator of approximately 40,000km due to a 0.5C change in temperature is approximately:

0.5 x 40,000 x 1000 x 5×10-6 = 100m

For a 100,000 year heating cycle that amounts to:

100/100,000 = 1mm/year

Which is comparable with plate tectonic movements which are in the range of 0-100mm annually. At the very least, the heating and cooling of the crust as a result of the ice-age cycle, must significantly increase or decrease the rate of movement of plates.

But, there is a much bigger problem. Whilst we might have assumed an average temperature change of the order of 0.5C, the surface will heat disproportionately more by around 10C, which is  20x the “average” heating, and so 20x the expansion forcing a massive 20mm of plate expansion if this happened over the full 100k time period, but much greater if rock is closer to the surface.

If we repeat the calculations with a 1km slice, the rate of heat flow increases 10x, the thermal mass reduces to 1/10 and so instead of 80,000 years, we are talking around 800 years and for a 3.1km slice, the time to warm by 0.5 is of the order of 8000 years, the time since the last ice age.

And, here lies the real crux of the issue. Different layers of the crust will be heating at different rates. The result is that changing temperature on the surface will create stresses in the earth that build up with greater surface temperature change and with longer periods of cooler/hotter climate.

These stresses will sooner or later result in movement in the earth. We see very similar effects in all structures, and a notable example is a house. As the house heats (or cools), the various materials expand (or contract) at different rates. The result is that sooner or later the stress is enough to cause movement to start, and once the movement starts, it continues until the force is insufficient to make it move, then there is a pause as the temperature continues to rise (fall) until the stress is again enough to initiate movement. The result is a series of punctuated movements which we hear as creaking. Because of the low mass of the materials and the rapid heating/cooling, the sound is audible. But in the case of the earth, these punctuated movements are literally movements in the form of earthquakes.

Upward buckling

Moreover, this thermal stress will move through the crust. Those layers nearest the surface temperature change will heat most rapidly tending to expand the surface layers and tending to exert a buckling force trying to force up the surface layers. But later, after the surface tensions have been “resolved” by earth quakes, those further down will begin to expand, creating an opposite buckling stress on the crust.

Differential stresses

Worse still, the different composite rocks of the crust have different rates of expansion. For example, sandstone has twice the rate of expansion of basalt, so a 1km section of basalt will expand 5mm less than a 1km section of sandstone for each degree centigrade change. That might no sound much, but over tens of kilometres, and with a 10 centigrade change, the total difference is around a meter, more than enough to cause a major earthquake.

An interplay between plate tectonics &climate?

So far this has been a purely passive response of the earth to the changes in surface temperature, but is it possible that plate tectonics could act the other way to affect affect climate?

If the crust of the earth expands due to temperature increase, then that crust can’t just get bigger, part of the crust will be forced down under adjacent plates so that the rocks of the crust expand but the total size of the crust remains the same.These rocks will be forced down into the mantel and then subject to huge temperatures and pressures. As many of these rocks will be carbon rich, the result will be to liberate many carbon containing chemicals including huge quantities of CO2 which will eventually make its way into the atmosphere (it may also create oil … but that’s another grand theory) … obviously CO2 causes more warming (wink) so, the rate of warming will increase resulting in run-away global warming and further expansion and subduction of crust releasing more CO2 – leading to the end of the world – which as it hasn’t happened suggests it will never happen. However, it is possible that subduction and release of CO2 could magnify the effect of a small but sustained period of warming as caused by solar cycle variation.

However, sooner or later the expansion will stop, the temperature will start to decline (possibly by external forcing such as the earth’s tilt) and then the planet crust will start to shrink. A shrinking crust will cause “gaps” in the crust through which the mantle will come resulting in the expansion of areas like the mid-Atlantic ridge, this will continually fill in the gaps as the crust shrinks and the rate of subduction will stop, reducing the level of CO2 given out by volcanic activity until the earth goes back through another warming cycle.

There have been many theories postulated to explain tectonic plate movement. I’ve never been entirely convinced by these, but just assumed that they were the best guess of the experts. But if you do the math(s) it turns out that regular heating/cooling cycle like the ice-age cycle could be a significant driver of plate movement. Indeed, the expansion of the near surface layers may be more important than deeper layers, because expansion of the near surface layers causes a downward buckling that tends to assist subduction and/or because cooler surface layers could be stiffer and so exert more force compared to deeper layers which are hotter under extreme pressure so more likely to behave like a plastic than a rigid solid.

So is it possible that the main reason for plate movement is due to a cycle of expansion/contraction of plate due to cyclic temperature changes. Moreover, if it were possible that the main impact of CO2 were as cooling gas (which it is in part!!)- or some other similar feedback mechanism were found, then the release of CO2 as the crust expands could result in a delayed cooling (due to the time the surface change takes to reach significant depths) which then drives the cycle into shrinking, allows the reduction in CO2, which then leads to warming, until you have a regular CO2 climate cycle of about 100,000 years, causing the bulk of plate movement. It’s contrary to all perceived notions of CO2 as a warming gas, but as CO2 is also an excellent emitter of IR and higher concentrations in the upper atmosphere would help radiate heat. it is just possible – but testing such a theory is well above my pay grade.

Why the theory is unlikely

Unfortunately, under such a model, you would expect to see periods of subduction/volcanic release of CO2 interspersed with periods of little volcanic activity and ridge building at expansion zones. And whilst, I’ve not done any research, there’s nothing to suggest it is happening.

Summary

The earth’s crust must expand due to changes in surface temperature, however the rate of change is extremely slow and of the order of 10,000 to 1,000,000 years depending on the depth of penetration. This makes it very unlikely that even after a century of significant warming that there will be any perceivable impact. However, the inter-glacial period is long enough and there is a sufficiently large temperature change so that this will cause significant and measureable stresses on the earth’s crust. One would expect tectonic plate subduction zones to be most active in the warming phase, and expansion zones in the cooling phase.

High-Resolution Phylogenetic Analysis of Southeastern Europe Traces Major Episodes of Paternal Gene Flow Among Slavic Populations

  1. Marijana Peričić*, 1 ,
  2. Lovorka Barać Lauc*, 1 ,
  3. Irena Martinović Klarić*,
  4. Siiri Rootsi,
  5. Branka Janićijević*,
  6. Igor Rudan§,
  7. Rifet Terzić,
  8. Ivanka Čolak,
  9. Ante Kvesić,
  10. Dan Popović*,
  11. Ana Šijački#,
  12. Ibrahim Behluli**,
  13. Dobrivoje Đorđevi憆,
  14. Ljudmila Efremovska††,
  15. Đorđe D. Bajec#,
  16. Branislav D. Stefanović#,
  17. Richard Villems and
  18. Pavao Rudan*

+ Author Affiliations


  1. *Institute for Anthropological Research, Amruševa 8, 10000 Zagreb, Croatia; Estonian Biocentre, University of Tartu, Tartu, Estonia; School of Public Health Andrija Štampar, University of Zagreb Medical School, Zagreb, Croatia; §University of Edinburgh Medical School, Edinburgh, Scotland; Medical Faculty, University of Tuzla, Tuzla, Bosnia and Herzegovina; Clinical Hospital Center “Bijeli Brijeg,” Mostar, Bosnia and Herzegovina; #Emergency Unit of Clinical Center of Serbia, Belgrade, Serbia and Montenegro; **Medical Faculty, University of Prishtina, Prishtina, Kosovo; and ††Medical Faculty, University of Skopje, Skopje, Macedonia
  1. E-mail: mpericic@luka.inantro.hr
  • Accepted May 30, 2005.

Abstract

The extent and nature of southeastern Europe (SEE) paternal genetic contribution to the European genetic landscape were explored based on a high-resolution Y chromosome analysis involving 681 males from seven populations in the region. Paternal lineages present in SEE were compared with previously published data from 81 western Eurasian populations and 5,017 Y chromosome samples. The finding that five major haplogroups (E3b1, I1b* (xM26), J2, R1a, and R1b) comprise more than 70% of SEE total genetic variation is consistent with the typical European Y chromosome gene pool. However, distribution of major Y chromosomal lineages and estimated expansion signals clarify the specific role of this region in structuring of European, and particularly Slavic, paternal genetic heritage. Contemporary Slavic paternal gene pool, mostly characterized by the predominance of R1a and I1b* (xM26) and scarcity of E3b1 lineages, is a result of two major prehistoric gene flows with opposite directions: the post-Last Glacial Maximum R1a expansion from east to west, the Younger Dryas-Holocene I1b* (xM26) diffusion out of SEE in addition to subsequent R1a and I1b* (xM26) putative gene flows between eastern Europe and SEE, and a rather weak extent of E3b1 diffusion toward regions nowadays occupied by Slavic-speaking populations.

Key words

Introduction

Southeastern Europe (SEE) has traditionally been viewed as a “bridge” (Childe 1958) between the Near East and temperate Europe or as a key area in the process of transition from hunter-gathering to agropastoral, farming societies in Europe (e.g., Ammerman and Cavalli-Sforza 1984; Renfrew 1987; Zvelebil and Lillie 2000). Recent phylogeographic analyses of Y chromosome E and J haplogroups indicate that southern Europe and the Balkans indeed could have been both the receptors and sources of gene flow during and after the Neolithic (Cruciani et al. 2004; Semino et al. 2004). The STR haplotype diversity of these two haplogroups is considerably younger than that of other Y chromosome haplogroups spread in Europe. Among the latter, haplogroup I, perhaps, most clearly represents the paternal genetic component of the pre-Neolithic Europeans. In contrast to E and J, haplogroup I is virtually absent in Middle East and West Asia (Semino et al. 2000), and two of its major subclades have frequency peaks in northern Balkans and Scandinavia (Rootsi et al. 2004). Semino et al. (2000) and Barać et al. (2003) hypothesized that, besides southwest Europe, the northern Balkans could have been another possible Last Glacial Maximum (LGM) refugium and a reservoir of M170.

In this study we first examined the extent and nature of SEE paternal genetic contribution to the European genetic landscape based on a high-resolution Y chromosome typing involving 681 unrelated males from four modern states, Croatia, Bosnia and Herzegovina, Serbia and Montenegro (including the province of Kosovo), and Macedonia (fig. 1). Second, we exploited available data on Y chromosome variation among different southern, western, and eastern Slavic-speaking populations in Europe to draw conclusions about possible origin of major paternal lineages in the Slavic gene pool. Finally, based on geography, we assessed patterns of Y chromosome diversity across SEE.

FIG. 1.— 

Map of the studied region and sample locations (1 = Zabok, 2 = Zagreb, 3 = Donji Miholjac, 4 = Delnice, 5 = Pazin, 6 = Dubrovnik, 7 = Zenica, 8 = Mostar, 9 = Široki Brijeg, 10 = Belgrade, 11 = Pristhina, 12 = Skopje).

Materials and Methods

We analyzed 681 males from seven populations from SEE and 5,017 Y chromosomes from 81 western Eurasian populations available from literature. Blood samples were collected from healthy unrelated adults after obtaining informed consent. DNA was extracted using the salting-out procedure (Miller, Dykes, and Polesky 1988).

The following set of biallelic markers was analyzed using restriction fragment length polymorphism (RFLP) or in/del assays according to published protocols: M9 (Whitfield, Sulston, and Goodfellow 1995), YAP (Hammer and Horai 1995), SRY-1523 (Whitfield, Sulston, and Goodfellow 1995) (SRY-1523 is equivalent to SRY10831 [Whitfield, Sulston, and Goodfellow 1995]), 92R7 (Mathias, Bayés, and Tyler-Smith 1994), 12f2 (Rosser et al. 2000), M170, M173, M89 (Underhill et al. 2000), and P37 (Y Chromosome Consortium 2002). The polymorphic single nucleotide polymorphism (SNP) underlying markers M26, M35, M67, M69, M78, M81, M82, M92, M102, M123, M172, M201 (Underhill et al. 2000), M223 (Underhill et al. 2001), M241, M242, M253 (Cinnioğlu et al. 2004), and SRY8299/4064 (Whitfield, Sulston, and Goodfellow 1995) were sequenced after polymerase chain reaction (PCR) amplification. PCR-amplified products were purified using shrimp alkaline phosphatase and exonuclease treatment following Kaessmann et al. (1999) and sequenced using the BigDye Terminator Version 3.1 Cycle Sequencing Kit (Applied Biosystems, Foster City, Calif.) on an ABI PRISM 310 Genetic Analyzer (Applied Biosystems) by using the DNA Sequencing Analysis Software Version 3.7 (Applied Biosystems). M9 was typed on all samples, and other markers were typed hierarchically according to their known phylogeny. A tentative assignment of all R1 chromosomes derived at M173 but without the G to A back mutation at SRY10831 into haplogroup R1b was based on the observations of Cruciani et al. (2002). Phylogenetic relationships of analyzed biallelic markers are presented in figure 2. Mutation labeling follows the Y Chromosome Consortium (2002).

FIG. 2.— 

Y chromosomal SNP tree and haplogroup frequencies (percent) in seven SEE populations. *Croatian mainland from Barać et al. (2003) was additionally genotyped for deeper resolution of I in Rootsi et al. (2004) and for E and J in the present study. E3b1α chromosomes were defined by A7.1 nine-repeat allele.

In addition, we surveyed eight short tandem repeats (STRs) DYS19, DYS385, DYS389I, DYS389II, DYS390, DYS391, DYS392, and DYS393 (Kayser et al. 1997) on all 681 SEE chromosomes and one additional GATA STR A7.1 (DYS460) (White et al. 1999) in E3b1-M78 chromosomes. PCR products were detected on an ABI PRISM 310 Genetic Analyzer (Applied Biosystems), and fragment sizes were analyzed by the GeneScan Analysis Software Version 3.7 (Applied Biosystems).

Expansion ranges were expressed as the age of STR variation estimated as the average squared difference in the number of repeats of seven STRs (DYS19, DYS389I, DYS389II, DYS390, DYS391, DYS392, and DYS393) between all sampled chromosomes and the founder haplotype divided by w (effective mutation rate of 0.00069 per locus per 25 years) (Zhivotovsky et al. 2004). Phylogenetic networks were obtained by using the same seven STRs as those used for expansion range estimates. The phylogenetic relationships between microsatellite haplotypes were determined by using the program NETWORK 4.0b (Fluxus Engineering). Networks were calculated by the median-joining method (Bandelt, Forster, and Röhl 1999), and STR loci were weighted according to Helgason et al. (2000). Haplogroup-frequency and haplogroup-variance surfaces were reconstructed following the Kringing procedure by use of the Surfer System (Golden Software), the frequency data reported in table 1 and variance data from this study and literature, as specified in figures 3–7. Credible regions (95% CRs) for haplogroup frequencies were calculated from posterior distribution of the proportion of the group of lineages in the population, as in Richards et al. (2000). For the purpose of correlating Y chromosomal frequencies with geography, we used Spearman’s bivariate correlation procedure (SPSS for Windows, 7.5.1.). Sampled individuals were pooled into 12 regional towns (fig. 1) with following latitude (N) and longitude (E) values: (1) 46°02′, 15°90′; (2) 45°82′, 15°98′; (3) 45°77′, 18°17′; (4) 45°40′, 14°80′; (5) 45°23′, 13°93′; (6) 42°65′, 18°09′; (7) 44°22′, 17°90′; (8) 43°35′, 17°80′; (9) 43°39′, 17°55′; (10) 44°82′, 20°46′; (11) 42°67′, 21°17′; and (12) 41°98′, 21°43′.

View this table: 

Table 1 

Summarized Percent Frequencies of R1b, R1a, I1b* (xM26), E3b1 and J2e

FIG. 3.— 

I1b* (xM26) frequency and variance surfaces in SEE (panels A and B) were generated from the data in this study. I1b* (xM26) frequency surfaces in Europe, northern Africa, and Asia Minor (panel C) were generated from the data reported in table 1, and variance surfaces (panel D) were generated from STR data in this study and Rootsi et al. (2004).

FIG. 4.— 

E3b1 frequency and variance surfaces in SEE (panels A and B) were generated from the data in this study. E3b1 frequency surfaces in Europe, northern Africa, and Asia Minor (panel C) were generated from the data reported in table 1, and variance surfaces (panel D) were calculated from STR data in this study and Semino et al. (2004).

FIG. 5.— 

R1a frequency and variance surfaces in SEE (panels A and B) were generated from the data in this study. R1a frequency surfaces in Europe, northern Africa, and Asia Minor (panel C) were generated from the data reported in table 1, and variance surfaces (panel D) were calculated from STR data in this study, Rootsi et al. unpublished data, Cinnioğlu et al. (2004), Behar et al. (2003), Weale et al. (2002), Wilson et al. (2001), Helgason et al. (2000), and Hurles et al. (1999). Shaded areas in panel D correspond to regions for which combined SNP and STR Y chromosomal data are not available.

FIG. 6.— 

R1b frequency and variance surfaces in SEE (panels A and B) were generated from the data in this study. R1b frequency surfaces in Europe, northern Africa, and Asia Minor (panel C) were generated from the data reported in table 1, and variance surfaces (panel D) were calculated from STR data in this study, Rootsi et al. unpublished data, Cinnioğlu et al. (2004), Behar et al. (2003), Weale et al. (2002), Wilson et al. (2001), Helgason et al. (2000), and Hurles et al. (1999). Shaded areas in panel D correspond to regions for which combined SNP and STR Y chromosomal data are not available.

FIG. 7.— 

J2e frequency and variance surfaces in SEE (panels A and B) were generated from the data in this study. J2e frequency surfaces in Europe, northern Africa, and Asia Minor (panel C) were generated from the data reported in table 1, and variance surfaces (panel D) were generated from STR data in this study and Semino et al. (2004).

Results and Discussion

One-third of the studied SEE Y chromosomes has the derived P37 C allele and is classified to haplogroup I1b* (xM26) (fig. 2). A detailed survey demonstrates that I1b* (xM26) lineages reach maximum frequency in SEE (fig. 3C) and that I1b* (xM26) STR variance peaks over a large geographic region encompassing both southeastern and central Europe (fig. 3D). I1b* (xM26) frequency peaks in Herzegovinians (64%) and Bosnians (52%) while preserving substantial (30%) frequencies in all SEE populations with the exception of two reproductively isolated and non-slavic speaking populations, Kosovar Albanians and Macedonian Romani (fig. 3A). The incidence of I1b* (xM26) decreases from SEE toward western (from 20% in Slovenians abruptly to 1% in northern Italians) and southern (17%–18% in Albanians and northern Greeks, 8% in southern Greeks, 2% in Turks) and retains frequencies of 7%–22% in central and eastern Europe (table 1). The highest STR variance of I1b* (xM26) lineages (0.34 to 0.23) is in Bosnians, Czechs and Slovaks, Hungarians, Herzegovinians, and Serbians (fig. 3B and D). In both cases, when all studied SEE populations are considered together and upon exclusion of Kosovar Albanians and Macedonian Romani, I1b* (xM26) frequency and variance do not show significant correlations with geography (table 2). Moreover, I1b* (xM26) phylogenetic network (fig. 8A) shows high haplotype diversity and sharing of founder haplotype among investigated populations. In fact, homogenous distribution of elevated frequency accompanied with high diversity of I1b* (xM26) lineages among different SEE populations may be viewed as a genetic signature of their common paternal history over a long period of time. Rootsi et al. (2004) estimated that I1b* (xM26) diverged from I* at 10.7 ± 4.8 kilo years ago (KYA), possibly relating to the post–Younger Dryas (YD) climate amelioration in Europe, and that I1b* (xM26) expansion occurred around the early Holocene at 7.6 ± 2.7 KYA. Considering only our SEE sample, the coalescent estimate of I1b* (xM26) is substantially older (11.1 ± 4.8 KYA). This finding suggests that the I1b* (xM26) lineages might have expanded from SEE to central, eastern, and southern Europe, presumably not earlier than the YD to Holocene transition and not later than the early Neolithic.

View this table: 

Table 2 

Correlations of Major Y Chromosome Haplogroup Frequencies and Variances with Geography

FIG. 8.— 

Microsatellite networks of major Y chromosomal lineages in SEE: (A) I1b* (xM26) (B) E3b1α; (C) R1a. Microsatellite haplotypes are represented by circles, with areas proportional to the number of individuals harboring the haplotype. Smallest circle represents single haplotype in panel B and C and two haplotypes in panel A. Branch lengths are proportional to the number of one-step mutations separating two haplotypes.

Haplogroup E3b1-M78 is the second most prevailing one (23%) in the studied sample with E3b1-M78 chromosomes accounting for almost all E representatives (98%) except a single E3b2-M81 and two E3b3-M123 chromosomes (fig. 2). E3b1-M78 is the most common haplogroup E lineage in Europe (Cruciani et al. 2004; Semino et al. 2004). The spatial pattern shown in figure 4(C) depicts a nonuniform E3b1 geographic distribution with a frequency peak centered in south Europe and SEE (13%–16% in southern Italians and 17%–27% in the Balkans). Declining frequencies are evident toward western (10% in northern and central Italians), central, and eastern Europe (from 4% to 10% in Polish, Russians, mainland Croatians, Ukrainians, Hungarians, Herzegovinians, and Bosnians). Noteworthy is a low E3b1 frequency (5%) in Turkey. Apart from its presence in Europe and the Middle East, E3b1 is also found in eastern and northern Africa. Cruciani et al. (2004) estimated that E3b-M78 might have originated in eastern Africa about 23.2 KYA (95% confidence interval [CI] 21.1–25.4). Although present level of phylogenetic resolution does not allow further subdivision of this haplogroup by binary markers, based on strong geographic structuring of diverse microsatellite motifs, E3b-M78 is suggested to be a collection of subclades with different evolutionary histories (Cruciani et al. 2004; Semino et al. 2004) out of which the α cluster, largely characterized by an A7.1 nine-repeat allele, is confined to Europe (the Balkans) and Turkey (Cruciani et al. 2004). E3b1 variance distribution depicted in figure 4(D) does not overlap with its frequency distribution possibly because analyzed E3b1 chromosomes harbor diverse background motifs. It is very likely that a variance peak centered in northeastern Africa as well as high variance values in Turkey and southern Italy are due to the inclusion of δ (and a few southern Italian β) chromosomes. Almost 93% of SEE E3b1 chromosomes are classified into α cluster. In Europe, the highest E3b1α variance is among Apulians, Greeks, and Macedonians, and the highest frequency of the cluster is among Albanians, Macedonians, and Greeks (table 1). Bearing in mind the congruent E3b1α frequency, variance maximums, and star-like phylogenetic network (fig. 8B), it is possible to envision that a yet undefined sublineage downstream of M78, characterized by the nine-repeat allele at A7.1 locus, may have originated in south Europe and SEE from where it dispersed in different directions. Furthermore, it may be envisioned that the observed E3b1α frequency distribution in Anatolia might stem from a back migration originating in south Europe and SEE. Our estimated range expansion of 7.3 ± 2.8 KYA is close to the 7.8 KYA (95% CI 6.3–9.2 KYA) estimate for expansions of cluster α chromosomes in Europe reported by Cruciani et al. (2004) and the 6.4 KYA estimate for E3b1-M78 STR variance in Anatolia dated by Cinnioğlu et al. (2004). The frequency and variance decline of E3b1 in SEE is rather continuous (fig. 4A and B), with a frequency peak extending from the southeastern edge of the region and a variance peak in southwest. Observed high E3b1 frequency in Kosovar Albanians (46%) and Macedonian Romani (30%) represent a focal rather than a clinal phenomenon resulting most likely from genetic drift. E3b1 frequency and variance are significantly correlated with latitude, showing higher values toward south (table 2), both when all SEE populations are considered (r = −0.51, P = 0.05, for frequency and r = −0.706, P = 0.05, for variance) and when Kosovar Albanians and Macedonian Romani are excluded (r = −0.597, P = 0.05, for frequency and r = −0.676, P = 0.05, for variance). A lower frequency of E3b1 significantly distinguishes populations of the Adriatic-Dinaric complex, i.e., mainland Croatians, Bosnians, and Herzegovinians (7.9%; 95% CI 0.054–0.114), from their neighboring populations of the Vardar-Morava-Danube river system, i.e., Serbians and Macedonians (21.9%; 95% CI 0.166–0.283). These observations hint a mosaic of different E3b1 dispersal modes over a short geographic distance and point to the Vardar-Morava-Danube river system as one of major routes for E3b1, in fact E3b1α, expansion from south and southeastern to continental Europe. In fact, dispersals of farmers throughout the Vardar-Morava-Danube catchments basin are also evidenced in the archaeological record (Tringham 2000).

R1a haplogroup occurs at 16% frequency in SEE (fig. 2). The age of M17 has been approximated to 15 KYA (Semino et al. 2000; Wells et al. 2001). Kivisild et al. (2003) suggested that southern and western Asia might be the source of R1 and R1a differentiation. Current R1a-M17/SRY-1532 distribution in Europe shows an increasing west-east frequency and variance gradients with peaks among Finno-Ugric and Slavic speakers (fig. 5C and D). Similar to I1b* (xM26), R1a frequency gradient decreases slowly to the south (to 10% in Albanians, 8% in Greeks, and 7% in Turks) and abruptly in the west (3% in Italians) (table 1). R1a frequency and STR variance decrease in the north-south direction in SEE, from 34%–25% in mainland Croatians and Bosnians to 12%–16% in Herzegovinians, Macedonians, and Serbians (fig. 5A and B). Moreover, R1a frequency is significantly correlated with latitude (table 2) when all studied SEE populations are considered (r = 0.865, P = 0.01) and also when Kosovar Albanians and Macedonian Romani are excluded (r = 0.743, P = 0.01). High R1a haplotype diversity in SEE is evident in the phylogenetic network (fig. 8C) and the estimated range expansion at 15.8 ± 2.1 KYA, consistent with its deep Paleolithic time depth, as previously suggested (Semino et al. 2000; Wells et al. 2001). At this level of resolution, it is not clear what temporal and effective population size differences contributed to this deep Paleolithic signal as high R1a variance in SEE might be explained by either ancient demography or more recent bottlenecks and founder effects in different Slavic tribes. At least three major episodes of gene flow might have enhanced R1a variance in the region: early post-LGM recolonizations expanding from the refugium in Ukraine, migrations from northern Pontic steppe between 3000 and 1000 B.C., as well as possibly massive Slavic migration from A.D. 5th to 7th centuries.

R1b haplogroup is present in SEE at a level of 9% (fig. 2). R1b-M173 lineages are considered to trace an Upper Paleolithic migration from West Asia to European regions then occupied by Aurignacian culture (Semino et al. 2000; Underhill et al. 2001; Wells et al. 2001). The spatial distribution of R1b lineages shows a frequency peak (40%–80%) in western Europe and a decrease in eastern (with the exception of 43% in the Ossetians) and southern Europe (fig. 6C), whereas R1b variance shows multiple peaks in West Europe and Asia Minor (fig. 6D). While R1b variance displays a clear-cut northwestern-southeastern decline in SEE (fig. 6B), R1b frequency decline continues from western toward southeastern and southern Europe, but two intermediate local peaks are evident, in north among mainland Croatians and Serbians and in south among Kosovar Albanians, Albanians, and Greeks (fig. 6C). These spatial patterns might be due to the fact that R1b lineages contain associated RFLP 49a,f ht 15 and 35 sublineages with opposite distributions possibly reflecting repeopling of Europe from Iberia and Asia Minor during the Late Upper Paleolithic and Holocene (Cinnioğlu et al. 2004). The overall R1b frequency distribution in the Balkan Peninsula suggests its possible arrival from two different source populations during recolonization of Europe. We estimated the range expansion of R1b lineages in SEE at 11.6 ± 1.4 KYA. Although R1b lineages could have accumulated STR variance before diffusion in SEE, it is significant that its estimated range expansion almost perfectly matches the coalescent estimate for the I1b* (xM26) lineages, pointing to the YD to Holocene transition as possibly a period when these two major Y chromosome lineages started to expand in the region.

Haplogroup J defined by a 12f2 polymorphism is subdivided into two major clades, J1-M267 and J2-M172 (Cinnioğlu et al. 2004). J2-M172 is more prevalent in Europe where at least five different lineages can be traced—J2e*-M102, J2e1-M241, J2*-M172, J2f*-M67, and J2f1-M92 (fig. 2, Semino et al. 2004). In SEE, the most frequent are J2e lineages that comprise 5% of all chromosomes, while J2f cluster, a predominant J2 cluster in Greeks and Italians (Di Giacomo et al. 2004), is present at a frequency less than 1% (fig. 2). Most likely due to genetic drift, Kosovar Albanians harbor a J2e frequency peak whereas variance maximum declines from the southeastern edge of the studied region (fig. 7A and B). Even though J2e frequencies do not correlate with geography, J2e variances show significant correlations with latitude and longitude and are highest toward south and east of the region (table 2). The correlation between geography and haplogroup frequencies are significant when all SEE populations are considered (r = −0.949, P = 0.05) and when Kosovar Albanians and Macedonian Romani are excluded (r = −0.949, P =0.05). Our estimated range expansion for J2e at 2.8 ±1.6 KYA (for all SEE populations) and 3 ± 1.9 KYA (SEE populations without Kosovar Albanians) succeeds the dates of 7.9 ± 2.3 KYA (Semino et al. 2004) and 8.6 KYA (Cinnioğlu et al. 2004). The J2e-M102 spatial distribution depicted in figure 7(C and D) with two frequency and variance peaks positioned in the Balkans and central Italy may be explained by the maritime spread of J2e lineages from southern Balkans toward Apennines at times later than those based on the classical model of demic expansions carried by Neolithic agriculturists from the Middle East via Balkans toward rest of Europe.

Widely spread Romani haplogroup H1 is a major lineage cluster in Macedonian Romani (fig. 2). A 2-bp deletion at M82 locus defining this haplogroup was also reported in one-third of males from traditional Romani populations living in Bulgaria, Spain, and Lithuania (Gresham et al. 2001). Its ancestral M52 A → C transversion was reported in the Vlax Roma (Kalaydjieva et al. 2001) and India (Ramana et al. 2001; Wells et al. 2001; Kivisild et al. 2003). Out of 34 H1-M82 males, 10 were typed for mitochondrial DNA (mtDNA) and belonged to haplogroup M that was highly frequent in Macedonian Romani (Cvjetan et al. 2004), traditional Romani populations (Gresham et al. 2001), and India (Kivisild et al. 2003). High prevalence of Asian-specific Y chromosome haplogroup H1 and mtDNA haplogroup M supports their Asian (Indian) origin and a hypothesis of a small number of founders diverging from a single ethnic group in India (Gresham et al. 2001).

F*, G-M201, K* (xP), P* (xR1, Q), and Q-M242 lineages occur at low frequencies in SEE (fig. 2). The Herzegovinian Q-M242 sample harbors a STR motif previously seen in eastern Adriatic haplogroup Q lineages that are marked by the typical presence of the unusually long DYS392-15 allele (Barać et al. 2003).

We conclude that even though the majority of identified SEE paternal lineages are consistent with the typical European Y chromosome gene pool, their distribution and estimated range expansions clarify the specific role of this region in structuring the European genetic landscape. Contemporary Slavic paternal gene pool is characterized by the predominance of R1a and I1b* (xM26) variants as well as the scarcity of E3b1 lineages as a result of the following prehistoric gene flows. First, we envision the post-LGM R1a expansion from eastern to western Europe and second the YD-Holocene I1b* (xM26) diffusion out of the Balkans in addition to subsequent R1a and I1b* (xM26) putative gene flows between eastern Europe and SEE. Lastly, we envision a weaker extent of E3b1 dispersal out of southern Europe and SEE toward eastern Europe rather than toward western (especially Mediterranean) Europe. Our results also stress that I1b* (xM26) wide geographic distribution and massive frequencies accompanied with high diversity in most of its range among major SEE populations testify impressively to their common paternal history, whereas observed genetic heterogeneity structured mostly along the northwestern-southeastern axis is a result of attested prehistoric and historical gene flows with different temporal and directional characteristics. Yet the main difference between the paternal genetic history of the Slavic-speaking populations lies in the presence, among eastern Slavs (Russians, Ukrainians, Belarussians), of haplogroup N chromosomes, virtually absent among any of the western or southern Slavic populations (Rosser et al. 2000; Semino et al. 2000; Barać et al. 2003; Tambets et al. 2004), unequivocally suggesting that the historic eastward expansion of Slavs in the middle of the first millennium A.D. resulted in a substantial admixture of them with the substratum populations, inhabiting East Europe, among whom this largely northern Eurasian haplogroup was and still is widely spread.

Acknowledgments

We are grateful to all the donors for their kind participation in this study. Special thanks go to Toomas Kivisild for friendly guidance and helpful comments for this manuscript. We wish to express our gratitude to two anonymous reviewers for their helpful suggestions. This research was supported by the Ministry of Science, Education and Sports of the Republic of Croatia grant for project 0196005 (to P.R.), Estonian basic research grant 514 (to R.V.), European Commission Directorate General Research grant ICA1CT20070006 (to R.V.), and Estonian Science Foundation grant number 6040 to Kristiina Tambets.

Footnotes

  • 1 The first two authors contributed equally to this study.

  • Lisa Matisoo-Smith, Associate Editor

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2 Responses to Global Warming and Earthquakes.

  1. Ian Youles says:

    My impression is that variations in heat flow from the centre of earth and the effects of isostasy with loading/unloading of ice would far outweigh any effects on the crust from atmospheric temperature changes. Wikipedia have an explanatory page at http://en.wikipedia.org/wiki/Post-glacial_rebound

    • Doesn’t that raise the intriguing possibility that ice-ages are caused by variations in heat from the crust?

      And thanks for the suggestion regarding ice loading. I wasn’t very happy with the use of CO2 as a feedback mechanism leading to a cyclic behaviour and it hadn’t occurred to me that there was a more obvious change due to temperature as huge lumps of ice begin compressing the surface around the poles.

      I’m going to have to think about it.

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