\makeatletter
\@ifundefined{HCode}
{\documentclass[screen,CRGEOS,Unicode]{cedram}
%\usepackage[sort&compress,square,comma,authoryear]{natbib}
\usepackage[square,comma,authoryear]{natbib}
\newenvironment{Table}{\begin{table}}{\end{table}}
\renewcommand\bibsection{\section*{\refname}}
\newenvironment{noXML}{}{}
\def\thead{\noalign{\relax}\hline}
\def\endthead{\noalign{\relax}\hline}
\def\tbody{\noalign{\relax}}
\def\tsup#1{$^{{#1}}$}
\def\tsub#1{$_{{#1}}$}
\def\0{\phantom{0}}
\usepackage[figuresright]{rotating}
\def\botline{\\\hline}
\def\tabnote#1{\vskip4pt\parbox{1\linewidth}{#1}}
\RequirePackage{etoolbox}
\usepackage{upgreek}
\def\jobid{crgeos20230775}
%\graphicspath{{/tmp/\jobid_figs/web/}}
\graphicspath{{./figures/}}
\newcounter{runlevel}
\usepackage{multirow} 
\def\nrow#1{\@tempcnta #1\relax%
\advance\@tempcnta by 1\relax%
\xdef\lenrow{\the\@tempcnta}}
\def\morerows#1#2{\nrow{#1}\multirow{\lenrow}{*}{#2}}
\let\MakeYrStrItalic\relax
\def\refinput#1{}
\def\back#1{}
\csdef{Seqnsplit}{\\}
\DOI{10.5802/crgeos.251}
\datereceived{2023-09-22}
\daterevised{2023-12-09}
\dateaccepted{2023-12-13}
\ItHasTeXPublished
\makeatletter
\g@addto@macro{\UrlBreaks}{\UrlOrds}
\gappto{\UrlBreaks}{\UrlOrds}
\def\inlinefig#1{\includegraphics{#1}}
\def\bcaption#1#2#3{\caption{Caption continued on next page.}\end{figure*}\setcounter{figure}{#2}\begin{figure*}\vspace*{-1pc}\caption{(\textbf{cont}.)\space#1\space #3}}
\gdef\tabularbreakone{\\ \hline
\multicolumn{14}{r@{}}{(continued on next page)\vspace*{-3pt}}
\end{tabular} 
\end{sidewaystable*}
\setcounter{table}{1}
\begin{sidewaystable*}
\vspace*{18pc}
\caption{(continued)}
\tabcolsep=3pt\fontsize{7.8}{10.5}\selectfont
\begin{tabular}{lccccccccccccc}
\thead
Sample$^{\mathrm{a}}$ & $^{\mathrm{b}}$ &
\parbox[t]{1cm}{\centering Latitude (\textdegree\ N)$^{\mathrm{c}}$} & 
\parbox[t]{.8cm}{\centering Long. (\textdegree\ E)$^{\mathrm{c}}$} &
\parbox[t]{1.8cm}{\centering Sample elevation above the river (m)} & 
\parbox[t]{1.6cm}{\centering Sample depth below the surface  (m)} &
Method$^{\mathrm{d}}$ & 
\parbox[t]{1.2cm}{\centering Lab-code reactor reference} &
\parbox[t]{1.2cm}{\centering $\mbox{}^{14}$C ages (ka)} & 
\parbox[t]{2.2cm}{\centering Calibrated interval $\mbox{}^{14}$C Cal ka BP (Probability $=$ 0.95)} & 
\parbox[t]{1cm}{\centering Ages (ka)$^{\mathrm{e}}$} &
\parbox[t]{1.2cm}{\centering Local terrace name} & 
\parbox[t]{1.1cm}{\centering Regional terrace name}\vspace*{2pt} & 
Source$^{\mathrm{f}}$ \\
\endthead
\vspace{-12pt}
}
\def\vspone{\vspace*{18pc}}
\def\vsptwo{\vspace*{17pc}}
}
{
\PassOptionsToPackage{authoryear}{natbib}
\documentclass[crgeos]{article}
\usepackage[T1]{fontenc} 
\def\CDRdoi{10.5802/crgeos.251}
\makeatletter
\def\CDRsupplementaryTwotypes#1#2{}
\def\selectlanguage#1{} 
\def\href#1#2{\url{#1}}
\newenvironment{sidewaystable*}{\begin{table*}}{\end{table*}}
\def\bcaption#1#2#3{\caption{#1\space#3}}
\let\tabularbreakone\relax
\let\vspone\relax
\let\vsptwo\relax
}
\makeatother

\begin{document}

\begin{noXML}

\TopicEF{Research article}{Article de recherche}

\RubricEF{Geomorphology}{G\'eomorphologie}

\shortrunauthors

\title{Fluvial terrace formation in mountainous areas: (1)~Influence of
climate changes during the last glacial cycle in  Albania}

\alttitle{Formation de terrasses fluviales dans les zones montagneuses:
(1) Influence des changements climatiques au cours du dernier cycle
glaciaire en Albanie}

\author{\firstname{Oswaldo} \lastname{Guzm\'{a}n}}
\address{Grupo de Investigaci\'{o}n en Ciencias de La Tierra y Clima, 
Universidad Regional Amaz\'{o}nica Ikiam, Muyuna, 
Ecuador}
\address{ISTerre, Universit\'{e} Grenoble Alpes, 
Universit\'{e} Savoie Mont Blanc, 
CNRS, IRD, Le Bourget du Lac, 
France}

\author{\firstname{Jean-Louis} \lastname{Mugnier}\CDRorcid{0000-0002-3403-7747}\IsCorresp}
\addressSameAs{2}{ISTerre, Universit\'{e} Grenoble Alpes, 
Universit\'{e} Savoie Mont Blanc, 
CNRS, IRD, Le Bourget du Lac, 
France}
\email[J.-L. Mugnier]{jemug@univ-smb.fr}

\author{\firstname{Riccardo} \lastname{Vassallo}\CDRorcid{0000-0003-2785-8835}}
\addressSameAs{2}{ISTerre, Universit\'{e} Grenoble Alpes, 
Universit\'{e} Savoie Mont Blanc, 
CNRS, IRD, Le Bourget du Lac, 
France}

\author{\firstname{Rexhep} \lastname{Ko\c{c}i}\CDRorcid{0000-0002-8766-543X}}
\address{Institute of Geosciences of the Polytechnical University of Tirana, 
Albania}

\author{\firstname{Julien} \lastname{Carcaillet}\CDRorcid{0000-0001-5909-0184}}
\addressSameAs{2}{ISTerre, Universit\'{e} Grenoble Alpes, 
Universit\'{e} Savoie Mont Blanc, 
CNRS, IRD, Le Bourget du Lac, 
France}

\author{\firstname{Fran\c{c}ois} \lastname{Jouanne}\CDRorcid{0000-0001-9374-7880}}
\addressSameAs{2}{ISTerre, Universit\'{e} Grenoble Alpes, 
Universit\'{e} Savoie Mont Blanc, 
CNRS, IRD, Le Bourget du Lac, 
France}

\keywords{\kwd{Fluvial sedimentation}
\kwd{Climatic and vegetation controls}
\kwd{River piracy}
\kwd{Late glacial cycle}
\kwd{Interstadials}
\kwd{\textit{In situ} produced $\mbox{}^{10}$Be dating}
\kwd{$\mbox{}^{14}$C dating}}

\altkeywords{\kwd{S\'{e}dimentation fluviale}
\kwd{Contr\^{o}les climatiques, contr\^{o}les par la v\'{e}g\'{e}tation}
\kwd{Capture fluviale}
\kwd{Stade tardi-glaciaire}
\kwd{Interstades}
\kwd{Datation $\mbox{}^{10}$Be \textit{in situ}}
\kwd{Datation $\mbox{}^{14}$C}}

\begin{abstract} 
This work analyses terraces formation from the case of Albanian rivers.
An allostratigraphy study of the fluvial terraces is combined with new
numerical dating. 30 $\mbox{}^{14}$C and 4 $\mbox{}^{10}$Be new dated
sites along four rivers and 45 ages previously acquired along three
other rivers were used to define terrace chronologies at the scale of
the whole Albania. Few terrace remnants are related to stages older
than the last glacial period and are older than  $194\pm19$~ka. Terrace
level (T1) includes plain-like terraces and T1 is related to a rapid
succession of valley incision and valley fill that occurred during the
warm Holocene climatic optimum. The other nine terrace levels (T2 to
T10) formed during the last glacial period (MIS 5d to end of MIS 2).
Terraces T2, T6 and T7 formed nearly synchronously with interstadial
transitions toward warmer and wetter conditions. The formation of
terraces T3, T4, T5 and T8 (${\textless}$60~ka) coincide with the warm
climatic excursions of the Heinrich events. This result suggests that
these short climatic events strongly punctuate the geomorphologic
dynamics of rivers in mountainous areas.\vspace*{-3pt}
\end{abstract}

\begin{altabstract} 
Ce travail analyse la formation des terrasses \`{a} partir du cas des
rivi\`{e}res albanaises. Une \'{e}tude allostratigraphique des
terrasses fluviales est associ\'{e}e \`{a} de nouvelles datations
num\'{e}riques. 30 nouveaux sites dat\'{e}s par $\mbox{}^{14}$C et 4
$\mbox{}^{10}$Be le long de quatre fleuves et 45 \^{a}ges
pr\'{e}c\'{e}demment acquis le long de trois autres fleuves ont
\'{e}t\'{e} utilis\'{e}s pour d\'{e}finir des chronologies de terrasses
\`{a} l'\'{e}chelle de l'ensemble de l'Albanie. Peu de vestiges de
terrasses li\'{e}s \`{a} des stades plus anciens que la derni\`{e}re
p\'{e}riode glaciaire ont \'{e}t\'{e} dat\'{e} et le plus ancien a 
$194\pm19$~ka. Le niveau des terrasses (T1) comprend des zones de
plaine et T1 est li\'{e} \`{a} une succession rapide d'incision de
vall\'{e}e et de remplissage de vall\'{e}e qui se sont produits pendant
l'optimum climatique chaud de l'Holoc\`{e}ne. Neuf autres niveaux de
terrasses (T2 \`{a} T10) se sont form\'{e}s au cours de la derni\`{e}re
p\'{e}riode glaciaire (MIS 5d \`{a} la fin de MIS 2). Les terrasses T2,
T6 et T7 se sont form\'{e}es de mani\`{e}re presque synchrone avec des
transitions interstadiales vers des conditions plus chaudes et plus
humides. La formation des terrasses T3, T4, T5 et T8
(${\textless}$60~ka) co\"{i}ncide avec les excursions climatiques
chaudes des \'{e}v\'{e}nements Heinrich. Ce r\'{e}sultat sugg\`{e}re
que ces \'{e}v\'{e}nements climatiques courts ponctuent fortement la
dynamique g\'{e}omorphologique des cours d'eau en zone montagneuse.
\end{altabstract} 

\thanks{NATO SFP 977993 and the Science for Peace team, Institut de
Recherche et Developement}

\maketitle

\twocolumngrid

\end{noXML}

\section{Introduction}\label{sec1}
A huge body of published works  [e.g. see the bibliography in 
\citealp{Cordieretal2017}] suggests that the formation of river
terraces, defined as flat surfaces above fluvial sediment, is affected
by climate. It has been demonstrated that, in general, river incision
took place at climatic transitions 
\citep[e.g.][]{Vandenberghe2003,Vandenberghe2015,BridglandWestaway2008,Antoineetal2016}.
Nonetheless, numerous studies show that terraces are not a simple
climatic proxy  \citep{Cordieretal2017,Schanzetal2018,Pazzaglia2022}
and numerous processes interact together in \mbox{terrace} \mbox{formation}
\citep{Starkel1994,Vandenberghe2003,Vandenberghe2015}. Furthermore, it
has been stressed that climatic\unskip\break 
variations must cross thresholds of
duration or magnitude to induce changes between erosion and deposition 
\citep[e.g.][]{Schumm1979,Vandenberghe2003}. The role of the succession
of the glacial/interglacial periods is classically described for major
fluctuations at 10$^{5}$ years scale 
\citep[e.g.][]{Starkel1994,Riser1999}. However, the role of shorter
time scale climatic fluctuations is frequently discussed from the
compilation of geochronologic studies distributed on very large areas 
\citep{Pazzaglia2022} but is usually poorly evidenced along single
rivers  \citep{Woodwardetal2008}.

Terrace levels, formed during the last glacial cycle, are widely
preserved along all the Albanian rivers 
\citep{Woodwardetal2008,Carcailletetal2009,Kocietal2018}. Albanian
river catchments  (Figure~\ref{fig1}) are located in an area where
large-scale controls (climate, tectonics or eustatism) can be
considered similar: the climate is Mediterranean  \citep{Ozenda1975},
the tectonics is controlled by the Adriatic subduction beneath
southeastern Europe  \citep{Roureetal2004} and all rivers have the same
base level fluctuations linked to the eustatism 
\citep{LambeckChappell2001}.

Many studies have already described the general morphology of terraces
\citep{Melo1961,Prifti1981,Prifti1984,PriftiMecaj1987,Lewinetal1991,Woodwardetal2008} 
and other studies have focused on the history of incision/uplift 
\citep{Carcailletetal2009,Guzmanetal2013,Gemignanietal2022}. But to
make progress in understanding the genesis of terraces, numerical
chronological constraints are necessary and are therefore proposed in
this article.

There was few ages for the river terraces preserved in the central and
northern part of Albania. Four $\mbox{}^{10}$Be and 21 $\mbox{}^{14}$C
new terrace ages, as well as geomorphological data, are reported in
this paper. These data are combined with previous results in order to
furnish an allostratigraphic/chronologic framework for the unit
deposition and terrace formation during the past  200~ka along 7
Albanian rivers. This enriched database supported by 70 numerical ages
is used to discuss the influence of climate changes on the genesis of
terraces.

\begin{figure*}
\includegraphics{fig01}
\bcaption{\label{fig1}}{0}{The rivers of Albania.  (a)~Topographic map of
Albania derived from the 90-m Shuttle Radar Topography Mission (SRTM)
digital elevation model. Watersheds of the seven main Albanian rivers
are bounded by black dashed lines. Dark diamonds indicate published data 
\citep{Lewinetal1991,Hamlinetal2000,Woodwardetal2001,Woodwardetal2008,Carcailletetal2009,Guzmanetal2013,Kocietal2018}, 
yellow circles ($\mbox{}^{14}$C dating) and green stars
($\mbox{}^{10}$Be dating) indicate the data obtained in this study. The
boxes show the location of Supplementary Information, Appendix~5 and
Figure~\ref{fig7}.  Core 1202 and 1204 in the Ohrid and Prespa lakes
refer to the work of 
\citet[][see Figure~\ref{fig9}]{Wagneretal2009,Wagneretal2010}.}
\vspace*{7pt}
\end{figure*}

\section{Methodology}\label{sec2}

Field surveys have been performed along all the rivers and the
allostratigraphic units  \citep{Hughes2010} were defined from an
analysis of the lithostratigraphy and the geometry of the interface
between Quaternary
sediment and bedrock. Thicknesses and
characteristics of the sedimentary units were observed in approximately
one thousand sites. The terrace extension at large scale was mapped on
the basis of field observations reported on topographic maps at the
1:25,000 scale \citep{InstitutinTopografikteUshtriseTirana1990},
30-m digital elevation models  \citep{SRTM2013} and satellite images
(image@2023CNES/Airbus, available on Google Earth).
\looseness=-1

\subsection{Dating of sedimentary units and terrace
surfaces}\label{sec2.2} 
In a first step, the relative chronology of the terraces was deduced
for each river from the geometric relationship between the mapped
terraces  \citep{Prifti1981,Prifti1984,PriftiMecaj1987}. The
correlation between the terrace remnants was performed by
reconstructing a regular paleo-river profile from the upstream to
downstream zones  \citep{Guzmanetal2013}. 

Although some relative methods, such as those based on the soil
chronosequence, can differentiate the age of Middle Pleistocene
sequences  \citep{RoweySiemens2021}, they were not used in this work:
in the studied area, a dozen levels of terraces are distributed over a
time period spanning one hundred thousand years 
\citep{Carcailletetal2009}, a temporal distribution not favorable to
the use of surface alteration as a time indicator  \citep{Rixhon2022}.
Furthermore, it has been shown that numeric dating is the best way to
compare terrace chronologies at a large scale  \citep{Woodwardetal2008}
and that absolute dating techniques are necessary to correlate terraces
with climatic stages  \citep{Schalleretal2016}. 

In a second step, the numeric ages of the terraces were determined. New
data were based on radiocarbon ($\mbox{}^{14}$C) and \textit{in situ}
produced $\mbox{}^{10}$Be dating. (See  Supplementary Information,
Appendix~1 and Appendix~2 for technical details.)

The $\mbox{}^{14}$C ages represent the death of organic material.
Samples consist of plant remains or charcoal, a few millimeters in size
(Supplementary Information, Figure~S1b in Appendix~1), which
are transported rapidly by rivers. Although there may be a delay
between plant death and final deposition, we consider $\mbox{}^{14}$C
ages to represent the age of sediment deposition. In order to exclude
an eolian origin, that has sometimes been suggested in the
Mediterranean area for the formation of the upper sub-unit of
fine-grained deposits 
\citep{Woodwardetal2008,Obrehtetal2014,Cremaschietal2015}, the samples
were taken from deposits also containing some coarse sands and small
gravels or from fine-grained lenses within the coarse material
(Supplementary Information, Figure~S1c, Appendix~1). Therefore most
$\mbox{}^{14}$C samples were collected close to the bottom of the upper
sub-unit (see Supplementary Information, 
Figure~S1a, Appendix~1).

The $\mbox{}^{10}$Be ages represent the exposure ages of the terrace
surfaces  \citep{GossePhillips2001}. The $\mbox{}^{10}$Be concentration
on the terrace surface was measured in samples formed of amalgamated
quartz clasts less than 5 cm in length. The attenuation of
$\mbox{}^{10}$Be at depth was analysed by sampling cobble samples along
one profile and amalgamated pebbles samples along another one 
\citep{GossePhillips2001}; the best fit profiles and their
uncertainties were then calculated using a Monte Carlo approach 
\citep{Hidyetal2010}\unskip\break
(Table~\ref{tab1}). In addition to the new
$\mbox{}^{10}$Be ages, the previously published $\mbox{}^{10}$Be ages
were re-calibrated following the same procedure  (Table~\ref{tab2}).

\begin{sidewaystable*}
\vspone
\caption{\label{tab1}Results of the $\mbox{}^{10}$Be analysis (see
Figure~\ref{fig6} and the Supplementary Information, 
Appendix~2)}
\begin{tabular}{ccccccccccc}
\thead
Sample & 
\parbox[t]{1.2cm}{\centering
Type of sample} & 
Lithology & 
\parbox[t]{1.2cm}{\centering
Latitude (\textdegree\ N)} & 
\parbox[t]{1.3cm}{\centering
Longitude (\textdegree\ E)} & 
\parbox[t]{1.2cm}{\centering
Altitude (m)} & 
\parbox[t]{1.2cm}{\centering
Depth (cm)} & 
\parbox[t]{1.2cm}{\centering
Shielding factor} & 
\parbox[t]{1.8cm}{\centering
$\mbox{}^{10}$Be concentration (10$^5$ at/g)} & 
\parbox[t]{1.2cm}{\centering
$\mbox{}^{10}$Be age (ka)} & 
Terrace
\vspace*{2pt}\\
\endthead
\multicolumn{11}{l}{Lower paleo-Devoll} \\
Shk-10 & Cobble & Quarzite & 41.0618 & 19.8685 & \065 & \030 & 0.998 & $0.77 \pm 0.07$ & $18.81 \pm 2.4$ & T3$_{(\mathrm{pa})}$ \\
Shk-11& Cobble& Granite& & & & \047& & $0.21\pm0.05$& &  \\
Shk-12& Amalgam.pebbles& Heterogeneous& & & & \075& & $0.61 \pm 0.03$ & &  \\
Shk-14& Cobble& Granite& & & & 157& & $0.47 \pm 0.06$& &  \\
Shk-16& Cobble& Granite& & & & 240& & $0.66 \pm 0.05$ & & \vspace*{6pt}\\
\multicolumn{11}{l}{Mat river-Uzal Dam} \\
Ma-03& Amalgam.pebbles& Heterogeneous & 41.6748& 19.9166& 183& \010& 0.998& $4.40 \pm 0.14$ & $100.8 \pm 9.4$ & T8$_{(\mathrm{ma})}$ \\
Ma-09& Amalgam.pebbles& Heterogeneous & & & & 285& & $0.52 \pm 0.06$& &  \\
Ma-08& Amalgam.pebbles& Heterogeneous & & & & 495& & $0.27 \pm 0.02$& &  \\
Ma-07& Amalgam.pebbles& Heterogeneous & & & & 590& & $0.26 \pm 0.01$& & \vspace*{6pt} \\
\multicolumn{11}{l}{Mat river-Livadhi} \\
Ma-04& Amalgam.pebbles& Heterogeneous& 41.5920& 20.0336& 262& \0\00& 1& $5.63 \pm 0.16$ & 
${\ge}112.32 \pm 10.3$& T8$_{(\mathrm{ma})}$\vspace*{6pt}\\
\multicolumn{11}{l}{Mat river-Burrel}  \\
Ma-06& Amalgam.pebbles& Heterogeneous & 41.6042& 20.0130& 322& \0\00& 1& 
$10.04 \pm 0.40$& ${\ge}193.92 \pm 19.3$& T9$_{(\mathrm{ma})}$ 
\botline
\end{tabular}
\tabnote{The depth profiles are from  T3$_{(\mathrm{pa})}$ and
T8$_{(\mathrm{ma})}$ (location of Shk-10 and Ma-03 on the Supplementary
Information, 
Appendix~5 and 
Figure~\ref{fig7}, respectively). Samples
Ma-04 and Ma-06 are amalgamated clasts collected at the top surface of
terraces T8$_{(\mathrm{ma})}$ and T9$_{(\mathrm{ma})}$, respectively
(location on Figure~\ref{fig7}).}
\end{sidewaystable*}

\begin{sidewaystable*}
\vsptwo
\caption{\label{tab2}Numeric ages from fluvial terraces of  Albania}
\tabcolsep=3pt\fontsize{7.8}{10.5}\selectfont
\begin{tabular}{lccccccccccccc}
\thead
Sample$^{\mathrm{a}}$ & $^{\mathrm{b}}$ &
\parbox[t]{1cm}{\centering Latitude (\textdegree\ N)$^{\mathrm{c}}$} & 
\parbox[t]{.8cm}{\centering Long. (\textdegree\ E)$^{\mathrm{c}}$} &
\parbox[t]{1.8cm}{\centering Sample elevation above the river (m)} & 
\parbox[t]{1.6cm}{\centering Sample depth below the surface  (m)} &
Method$^{\mathrm{d}}$ & 
\parbox[t]{1.2cm}{\centering Lab-code reactor reference} &
\parbox[t]{1.2cm}{\centering $\mbox{}^{14}$C ages (ka)} & 
\parbox[t]{2.2cm}{\centering Calibrated interval $\mbox{}^{14}$C Cal ka BP (Probability $=$ 0.95)} & 
\parbox[t]{1cm}{\centering Ages (ka)$^{\mathrm{e}}$} &
\parbox[t]{1.2cm}{\centering Local terrace name} & 
\parbox[t]{1.1cm}{\centering Regional terrace name}\vspace*{2pt} & 
Source$^{\mathrm{f}}$ \\
\endthead
\multicolumn{14}{l}{Vjosa}\vspace*{4pt}  \\
A153 &  C &  40.2076 &  20.3875 &  17.3 &  0.7 &  $\mbox{}^{14}$C &  SacA
16001 &  $190 \pm 30$ &  32--302 &  - &  - &  colluv. &  This study \\
A150 &  C &  40.2084 &  20.0934 &  9.5 &  0.5 &  $\mbox{}^{14}$C &  SacA
15998 &  $330 \pm 30$ &  308--473 &  - &  - &  colluv. &  (1) \\
A28 &  Vd &  40.3354 &  19.9921 &  12 &  2 &  $\mbox{}^{14}$C &  Poz-8824 & 
$705 \pm 30$ &  565--691 &  - &  - &  colluv. &  (1) \\
OxA-192 &  C &  39.97(\c{c}) &  20.66(\c{c}) &  ${\sim}$4.5  & 
${<}$1 &  $\mbox{}^{14}$C &  OxA-192 &  $800 \pm 100$ & 
560--928 & - &  T1$_{(\mathrm{vj})}$ &  T0 &  (3) \\
OxA-191 &  C &  40.87(\c{c}) &  21.65(\c{c}) &  ${\sim}$4.5 & 
${<}$1 &  $\mbox{}^{14}$C &  OxA-191 &  $1000 \pm 50$ & 
789--1049 &  - &  T1$_{(\mathrm{vj})}$ &  T0 &  (3) \\
A155 &  Vd &  40.3611 &  19.9907 &  13.4 &  4 &  $\mbox{}^{14}$C &  SacA
16002 &  $3870 \pm 60$ &  4094--4436 &  - &  - &  colluv. &  (1) \\
OxA-5246 &  C &  39.96(\c{c}) &  20.65(\c{c}) &  ${\sim}$10.6 & 
${\sim}$0.1 &  $\mbox{}^{14}$C &  OxA-5246 &  $13810 \pm  130$
&  16,291--17,116 &  - &  T3$_{(\mathrm{vj})}$ &  T3 &  (4) \\
Beta-109162 &  C &  39.96(\c{c}) &  20.65(\c{c}) &  ${\sim}$10.6 & 
${\sim}$0.1 &  $\mbox{}^{14}$C &  Beta-109162 
&  $13960 \pm 260$ &  16,203--17,647 &  - &  T3$_{(\mathrm{vj})}$ &  T3 & (4) \\
Beta-109187 &  C &  39.96(\c{c}) &  20.65(\c{c}) &  ${\sim}$10.4 & 
${\sim}$0.4 &  $\mbox{}^{14}$C &  Beta-109187 &  
$14310 \pm 200$ &  16,865--17,947 &  - &  T3$_{(\mathrm{vj})}$ &  T3 &  (4) \\
VOI24 &  S &  39.94(\c{c}) &  20.71(\c{c}) &  ${\sim}$9.7 & 
${<}$1 &  TL &  VOI24 &  - &  - &  $19.60 \pm 3.00$ & 
T3$_{(\mathrm{vj})}$ &  T3 &  (3) \\
Tributary site &  Cc &  39.95(\c{c}) &  20.68(\c{c}) &  ${\sim}$10.5 
&  ${\sim}$1.6 &  U/Th &  - &  - &  - &  $21.25 \pm 2.50$ 
& T3$_{(\mathrm{vj})}$ &  T3 &  (5) \\
Old Klithonia &  Cc &  39.96(\c{c}) &  20.65(\c{c}) &  ${\sim}$9.3 &
${\sim}$2.3 &  U/Th &  - &  - &  - &  $24.00 \pm 2.00$ & 
T4$_{(\mathrm{vj})}$ &  T4 &  (5) \\
571c &  Dt &  39.96(\c{c}) &  20.68(\c{c}) &  ${\sim}$12.4 & 
${\sim}$7.5 &  ESR &  571c &  - &  - &  $24.30 \pm 2.60$ & 
T4$_{(\mathrm{vj})}$ &  T4 &  (3) \\
571a &  Dt &  39.96(\c{c}) &  20.68(\c{c}) &  ${\sim}$12.4 & 
${\sim}$7.5 &  ESR &  571a &  - &  - &  $25.00 \pm 0.50$ & 
T4$_{(\mathrm{vj})}$ &  T4 &  (3) \\
Old Klithonia &  Cc &  39.96(\c{c}) &  20.65(\c{c}) &  ${\sim}$9.3 &
${\sim}$5 &  U/Th &  - &  - &  - &  $25.00 \pm 2.00$ & 
T4$_{(\mathrm{vj})}$ &  T4 &  (5) \\
571b &  Dt &  39.96(\c{c}) &  20.68(\c{c}) &  ${\sim}$12.4 & 
${\sim}$7.5 &  ESR &  571b &  - &  - &  $26.00 \pm 1.90$ & 
T4$_{(\mathrm{vj})}$ &  T4 &  (3) \\
VOI23 &  S &  39.96(\c{c}) &  20.68(\c{c}) &  ${\sim}$12.4 & 
${<}$1 &  TL &  VOI23 &  - &  - &  $28.00 \pm 7.10$ ({\pounds}) &
T4$_{(\mathrm{vj})}$ &  T4 &  (3) \\
A151 &  C &  40.2140 &  20.3842 &  21.7 &  0.3 &  $\mbox{}^{14}$C &  SacA
15999 &  $24070 \pm 150$ &  27,783--28,848 &  - & 
T5$_{(\mathrm{vj})}$ &  T5 &  This study \\
Konitsa1 &  Cc &  39.86(\c{c}) &  20.77(\c{c}) &  ${\sim}$10 & 
${\sim}$1--1.5 &  U/Th &  - &  - &  - &  $53.00 \pm 4.00$ & 
T6$_{(\mathrm{vj})}$ &  T8 &  (5) \\
Konitsa2 &  Cc &  39.86(\c{c}) &  20.77(\c{c}) &  ${\sim}$10 & 
${\sim}$1-1.5 &  U/Th &  - &  - &  - &  $56.50 \pm 5.00$ & 
T6$_{(\mathrm{vj})}$ &  T8 &  (5) \\
Konitsa3 &  Cc &  39.86(\c{c}) &  20.77(\c{c}) &  ${\sim}$11 & 
${\sim}$1--1.5 &  U/Th &  - &  - &  - &  $74.00 \pm 6.00$ & 
T7$_{(\mathrm{vj})}$ &  T9 &  (5) \\
Konitsa4 &  Cc &  39.86(\c{c}) &  20.77(\c{c}) &  ${\sim}$12.7 & 
${\sim}$1--1.5 &  U/Th &  - &  - &  - &  $80.00 \pm 7.00$ & 
T7$_{(\mathrm{vj})}$ &  T9 &  (5) \\
Konitsa5 &  Cc &  39.86(\c{c}) &  20.77(\c{c}) &  ${\sim}$15.5 & 
${\sim}$1--1.5 &  U/Th &  - &  - &  - &  $113.00 \pm 6.00$ & 
T8$_{(\mathrm{vj})}$ &  T10 &  (5) \\
VOI26 &  S &  39.86(\c{c}) &  20.77(\c{c}) &  ${\sim}$56 & 
${\sim}$22 &  TL &  VOI26 &  - &  - &  ${>}$150({\pounds}) 
&  T9$_{(\mathrm{vj})}$ &  T12  &  (3)\tabularbreakone\\
\multicolumn{14}{l}{Osum} \vspace*{4pt}  \\ 
A17 &  Vd &  40.4508 &  20.2808 &  17 &  2 &  $\mbox{}^{14}$C &  Poz-10576 & 
$9990 \pm 50$ &  11,263--11,705  &  - &  T2$_{(\mathrm{os})}$ & T2 &  (2) \\
Par-0 (*) &  Sr &  40.5200 &  20.7200 &  70 &  0 &  $\mbox{}^{10}$Be 
&  - & - &  - &  $19.25 \pm 1.3$ &  T3$_{(\mathrm{os})}$ &  T3 &  (2) \\
Quaf-0 (*) &  Sr &  40.5500 &  20.6900 &  29 &  0 &  $\mbox{}^{10}$Be 
&  - & - &  - &  $20.33 \pm 1.5$ &  T3$_{(\mathrm{os})}$ &  T3 &  (2) \\
A16 &  Vd &  40.6394 &  20.0553 &  24 &  4 &  $\mbox{}^{14}$C &  Poz-10575 & 
$29900 \pm 1300$ &  31,323--37,457 &  - &  T5$_{(\mathrm{os})}$ &  T6 &  (2) \\
A83 &  C &  40.6800 &  20.0200 &  14.8 &  3.7 &  $\mbox{}^{14}$C &  Poz-13850
&  $37000 \pm 300$ &  41,036--42,066 &  - &  T6$_{(\mathrm{os})}$ &  T7 & (2) \\
A18 &  Vd &  40.5600 &  20.1400 &  53 &  6 &  $\mbox{}^{14}$C &  Poz-10578 & 
$45300 \pm 1600$ &  ${>}$46237 &  $50.70 \pm 1.80$ (\$) & 
T7$_{(\mathrm{os})}$ &  T8 &  (2) \\
A14 &  Vd &  40.6403 &  20.0575 &  33.8 &  1.2 &  $\mbox{}^{14}$C &  Poz-10574
&  $49000 \pm 2500$ &  ${>}$49928 &  $54.40 \pm 2.78$ ({\$}) & 
T7$_{(\mathrm{os})}$ &  T8 &  (2) \\
Grem-0(*) &  Sr &  40.5560 &  20.7383 &  50 &  0 
&  $\mbox{}^{10}$Be & - & - & - &  $54.01 \pm 3.0$ 
&  T7$_{(\mathrm{os})}$ &  T8 \vspace*{6pt} &  (2) \\ 
\multicolumn{14}{l}{Paleo-Devoll}\vspace*{4pt} \\  
A05 &  Vd &  40.9092 &  20.1393 &  34 &  2 &  $\mbox{}^{14}$C &  Poz-10572 & 
$119.5 \pm 0.3$ pMC &  - &  modern &  - &  colluv. &  This study \\
Cer-08 &  C &  41.0275 &  19.9817 &  8.4 &  0.6 &  $\mbox{}^{14}$C & 
Poz-39495 &  $30 \pm 80$ &  9--275 &  - &  - &  colluv. &  (1) \\
Dev-02 &  C &  40.9910 &  20.0165 &  16.6 &  0.5 &  $\mbox{}^{14}$C & 
Poz-39496 &  $540 \pm 130$ &  306--727 &  - &  - &  colluv. &  (1) \\
Shk-06 &  Vd &  41.0663 &  19.8800 &  52.8 &  2.2 &  $\mbox{}^{14}$C & 
Poz-34987 &  $162 \pm 0.46$ pMC &  &  modern &  - 
&  colluv. &  This study \\
Shk-22 &  C &  41.0649 &  19.8714 &  6.3 &  0.7 &  $\mbox{}^{14}$C & 
Poz-39201 &  $90 \pm 30$ &  22--266 &  - & - &  colluv. &  This study \\
Cer-01 & C &  41.0100 &  20.0083 &  8.4 &  1.6 &  $\mbox{}^{14}$C &  Poz-39197 
&  $5400 \pm 40$ &  6021--6293 &  - &  T2$_{(\mathrm{pa})}$ &  T1 &  This study \\
Shk-10(*) &  Sr  &  41.0618 &  19.8685 &  14.7 &  0.3 & 
$\mbox{}^{10}$Be &  - &  - &  &  $18.81 \pm 2.4$ & 
T3$_{(\mathrm{pa})}$ &  T3 &  This study \\
A60 &  C &  40.9676  &  20.0526  &  19 &  0.5 &  $\mbox{}^{14}$C &  Poz-12223 
&  $17640 \pm 160$  &  20,895--21,800 &  - &  T3$_{(\mathrm{pa})}$ &  T3 &  (1) \\
A58 &  C &  40.9214  &  20.1292  &  15.7 &  3 &  $\mbox{}^{14}$C &  Poz-12116 
&  $21850 \pm 150$  &  25,815--26,437 &  - &  T4$_{(\mathrm{pa})}$ &  T4 &  (1) \\
A100 &  C &  40.9660  &  20.0636  &  24 &  1 &  $\mbox{}^{14}$C &  Poz-17242 
&  $22780 \pm 200$  &  26,583--27,490 &  - &  T4$_{(\mathrm{pa})}$ &  T4 &  (1) \\
A8 &  Vd &  40.8271  &  20.2154  &  42.5 &  5 &  $\mbox{}^{14}$C &  Poz-9838 
&  $23760 \pm 150$  &  27,580--28,163 &  - &  T5$_{(\mathrm{pa})}$ &  T5 & (1) \\
A1 &  Vd &  40.8836  &  20.1773  &  42 &  6 &  $\mbox{}^{14}$C &  Poz-8816  & 
$25500 \pm 300$  &  28,921--30,498 &  - &  T5$_{(\mathrm{pa})}$ &  T5 & This study \\
A61 &  C &  40.9414  &  20.1089  &  41.2 &  1 &  $\mbox{}^{14}$C &  Poz-12117 
&  $38900 \pm 700$  &  41,939--44,142 &  - &  T7$_{(\mathrm{pa})}$ &  T7 & This study \\
A56A &  C &  40.8834  &  20.1764  &  41 &  3 &  $\mbox{}^{14}$C &  & 
${>}$52000  &  &  ${>}$52 &  T8$_{(\mathrm{pa})}$ &  T8\vspace*{6pt} &  This study \\ 
\multicolumn{14}{l}{Erzen}\vspace*{4pt} \\ 
A41 &  C &  41.2697 &  19.8400 &  3 &  1.5 &  $\mbox{}^{14}$C &  Poz-8826  & 
$170 \pm 30$  &  35--291 &  - &  - &  colluv. &  (6) \\
A11 &  C &  41.2900 &  19.7100 &  3.4 &  0.8 &  $\mbox{}^{14}$C &  Poz-8818  &
$200 \pm 30$  &  25--304 &  - &  - &  colluv. &  (6) \\
A81 &  C &  41.2866  &  19.7094  &  23.4 &  1 &  $\mbox{}^{14}$C &  Poz-13849 
&  $275 \pm 35$  &  152--459 &  - &  - &  colluv. &  This study \\
A65 &  C &  41.3088  &  19.7544  &  29 &  0.8 &  $\mbox{}^{14}$C &  Poz-12784 
&  $500 \pm 30$  &  501--617 &  - &  - &  colluv. &  This study \\
A76 &  Vd &  41.2800  &  19.8300  &  11.7 &  1 &  $\mbox{}^{14}$C &  Poz-13847
&  $3075 \pm 35$  &  3182--3372 &  - &  - &  colluv. &  This study 
\tabularbreakone\\
A63B &  C &  41.2870  &  19.7197  &  17 &  3 &  $\mbox{}^{14}$C &  Poz-12118 
&  $3700 \pm 35$  &  3927--4150 &  - &  - &  colluv. &  This study \\
A13 &  C &  41.2700  &  19.6400  &  9 &  0.4 &  $\mbox{}^{14}$C &  Poz-8823  &
$1660 \pm 30$  &  1421--1690 &  - &  T1$_{(\mathrm{er})}$ &  T0 &  (6) \\
A12 &  C &  41.2700  &  19.6400  &  9 &  1 &  $\mbox{}^{14}$C &  Poz-10573  & 
$1730 \pm 30$  &  1564--1708 &  - &  T1$_{(\mathrm{er})}$ &  T0 &  This study \\
A42 &  Vd &  41.2700  &  19.8000  &  12 &  1 &  $\mbox{}^{14}$C &  Poz-8827  &
$6840 \pm 60$  &  7578--7817 &  - &  T2$_{(\mathrm{er})}$ &  T1 &  (6) \\
A115 &  C &  41.2844  &  19.9683  &  17 &  0.8 &  $\mbox{}^{14}$C &  Poz-17243
&  $26600 \pm 500$  &  29,631--31,465 &  - &  T3$_{(\mathrm{er})}$ &  T5 &  This study \\
A67 &  C &  41.2700  &  19.6400  &  9.4 &  3 &  $\mbox{}^{14}$C &  Poz-12120 
&  $30400 \pm 300$  &  33,889--34,912 &  - &  T4$_{(\mathrm{er})}$ &  T6 &  This study \\
A69 &  C &  41.2900  &  19.6400  &  41 &  1.2 &  $\mbox{}^{14}$C &  Poz-12121 
&  $31500 \pm 400$  &  34,671--36,231 &  - &  T4$_{(\mathrm{er})}$ &  T6 &  (6) \\
A64 &  C &  41.2700  &  19.7100  &  24.8 &  0.8 &  $\mbox{}^{14}$C & 
Poz-12224  &  $33400 \pm 500$  &  36,358--38,827 &  - & 
T4$_{(\mathrm{er})}$ &  T6 &  This study \\
A79 &  C &  41.2900  &  19.7100  &  26.5 &  2 &  $\mbox{}^{14}$C &  Poz-13848 
&  $44200 \pm 1600$  &  ${>}$45447 &  $49.59 \pm 1.76$({\$}) & 
T6$_{(\mathrm{er})}$ &  T8 &  This study \\
A70 &  C &  41.2900  &  19.6000  &  22 &  0.5 &  $\mbox{}^{14}$C &  Poz-12785 
&  $48000 \pm 2000$  &  ${>}$49910 &  $53.40 \pm 2.22$({\$}) & 
T6$_{(\mathrm{er})}$ &  T8\vspace*{6pt} &  (6) \\ 
\multicolumn{14}{l}{Mat}\vspace*{4pt} \\ 
Ma-05 &  C &  41.6178 &  20.0294 &  24.3 &  0.7 &  $\mbox{}^{14}$C & 
Poz-34984 &  $1075 \pm 30$ &  931--1056 &  - &  - &  colluv. &  This study \\
Ma-18 &  C &  41.6245 &  19.9978 &  7 &  0.7 &  $\mbox{}^{14}$C &  Poz-39198 &
$1725 \pm 30$  &  1562--1706 &  - &  T1$_{(\mathrm{ma})}$ &  T0 &  This study \\
Ma-21 &  C &  41.6246 &  19.9970 &  10.3 &  0.7 &  $\mbox{}^{14}$C & Poz-39199 
&  $5100 \pm 40$  &  5746--5922 &  - &  T2$_{(\mathrm{ma})}$ &  T1 &  This study \\
Ma-24 &  C &  41.6273 &  19.9968 &  26 &  2.1 &  $\mbox{}^{14}$C &  Poz-39200
&  $14850 \pm 80$ &  17,856--18,296 &  - &  T3$_{(\mathrm{ma})}$ &  T3 & This study \\
Ma-04(*) &  Sr &  41.5920 &  20.0336 &  100 &  0 &  $\mbox{}^{10}$Be
&  - &  - &  - &  $100.8 \pm 9.4$ &  T8$_{(\mathrm{ma})}$ &  T10 & This study \\
Ma-03 &  Sr &  41.6748 &  19.9166 &  94 &  0.1 &  $\mbox{}^{10}$Be & 
- &  - &  - &  $\ge 112.32  \pm 10.3$ &  T8$_{(\mathrm{ma})}$ & T10 &  This study \\
Ma-06 &  Sr &  41.6042 &  20.0130 &  190 &  0 &  $\mbox{}^{10}$Be & 
- &  - &  - &  $\ge 193.92  \pm 19.3$ &  T9$_{(\mathrm{ma})}$ & T11\vspace*{6pt} &  This study \\ 
\multicolumn{14}{l}{Drin}\vspace*{4pt} \\ 
TPN(*) &  Ca &  42.37855 &  20.08971 &  12 &  0.5 &  $\mbox{}^{36}$Cl
&  - &  - &  - &  8.2 ($-2/+4$)  &  T2$_{(\mathrm{dr})}$ &  T1 &  (7) \\
TPS(*) &  Ca &  42.34380 &  20.11545 &  56 &  0.4 &  $\mbox{}^{36}$Cl
&  - &  - &  - &  12.3 ($-2/+5$) &  T3$_{(\mathrm{dr})}$ &  T2 &  (7) 
\botline
\end{tabular}
\tabnote{$^{\mathrm{a}}$Samples: $(^{*})$ for a cosmogenic depth profile, only the age of
the surface and the depth of the shallowest sample are given. 
$^{\mathrm{b}}$Type of material dated: C $=$ charcoal, 
Vd $=$ vegetal debris, 
Cc $=$ calcite cement, 
S $=$ sediment, 
Dt $=$ deer tooth, 
Sr $=$ siliceous rock, 
Ca $=$ Calcereous rock. 
$^{\mathrm{c}}$Location from GPS coordinates or (\c{c}) estimated from published
maps.
$^{\mathrm{d}}$Dating method: $\mbox{}^{14}$C $=$ radiocarbon, 
TL $=$ thermoluminescence, 
U/Th $=$ uranium series, 
ESR $=$ electron spin resonance,
$\mbox{}^{10}$Be and $\mbox{}^{36}$Cl $=$ cosmogenic in situ produced data.
$^{\mathrm{e}}$Numerical ages: all $\mbox{}^{10}$Be ages have been calculated 
(Table~\ref{tab1})  or recalculated with the parameters indicated in
Supplementary Information,
Appendix~2. 
All $\mbox{}^{14}$C ages have been estimated from the
IntCal 13 calibrated intervals and the oldest (\$) were also corrected
using the polynomial calibration of  \citet{Bardetal2004}. ({\pounds})
Have not been considered for the probability density curves due to
their large uncertainty.
$^{\mathrm{f}}$Source: (1)~\citet{Guzmanetal2013}, 
(2)~\citet{Carcailletetal2009}, 
(3)~\citet{Lewinetal1991}, 
(4)~\citet{Woodwardetal2008},
(5)~\citet{Hamlinetal2000}, 
(6)~\citet{Kocietal2018}, 
(7)~\citet{Gemignanietal2022}.}
\end{sidewaystable*}

The limestone pebble-rich terraces of the Drin River 
\citep{Gemignanietal2022} have been dated using $\mbox{}^{36}$Cl. Other
ages  \citep{Lewinetal1991,Woodwardetal2008} refer to the mineral
formation (U/Th) or the time without daylight exposure (ESR and TL)
within the alluvium and are older than the ultimate phases of river
aggradation  \citep{Nolleretal2000}. 

\begin{figure*}
\includegraphics{fig02}
\caption{\label{fig2}Examples of sedimentary units and terraces in
Albania. (a)~Remnant of a fill terrace (T10$_{(\mathrm{vj})}$),  middle
section of the Vjosa River; (b)~Debris flow deposited above
T5$_{(\mathrm{vj})}$ terrace.}
\end{figure*}

\section{Setting}\label{sec3} 

\subsection{Climate and paleoclimate of Albania}\label{sec3.1}  
Albania's present climate is Mediterranean on the coast, with 2 to 3
hot, dry months in summer and 4 to 5 mild, rainy months in winter. In
the mountainous regions, the climate is continental with cold and
snow-covered winters. 

The paleo climatic records for the last 500~ka were studied in the
region in Lake Ohrid,  \citep{Sadorietal2016} and Lake Ioannina 
\citep{Roucouxetal2008} (location on  Figure~\ref{fig1}). These local
records correspond well with the results found in the isotope record of
Greenland  \citep{Grootesetal1993} or in the marine records of the
Iberian margin  \citep{deAbreuetal2003} and the eastern Mediterranean 
\citep{Konijnendijketal2015}. They show a succession of cold periods
followed by rapid warm excursions \citep{ClementPeterson2008}. 

The Adriatic Sea, which controls the base level of Albania's rivers,
was affected by eustatic fluctuations which are tuned to the global sea
level variations and ranged from  ${-}$120~m to ${+}$10~m during the last
glacial period  \citep{LambeckChappell2001}. Colder sea surface
temperatures that occurred in the Mediterranean Sea 
\citep{Cachoetal1999,SanchezGonietal2002,Geragaetal2005} during Marine
Isotope Stages (MIS) 5 to 2 were linked to the polar water that entered
through the Strait of Gibraltar and were closely related to ice rafting
events in the northeast Atlantic, called Heinrich events (HEs)
\citep{Heinrich1988}. These short cold events [one to two thousand
years;  \citealp{Chappell2002,Ziemenetal2019}] or even less 
\citep{Bondetal1992,Hemming2004} were always followed by warm periods
\citep{Rahmstorf2002}. Therefore, the temperature evolution of the
Albanian region at the millennial scale is similar to that of the north
Atlantic domain  \citep[e.g.][]{SanchezGonietal2002,Tzedakisetal2004}. 

The climatic-water-balance of the landscape (ratio between rainfall,
runoff, evapotranspiration, etc.) induces complex connection between
temperature and precipitation within the region and a decline in
precipitation probably occurred in the western Mediterranean Sea during
the Heinrich events. They induced cooler sea surface 
temperatures 
that\unskip\break
inhibited 
the moisture supply to the atmosphere 
\citep{Kalleletal1997,Kalleletal2000} whereas increased rainfalls in
the western Mediterranean region are evidenced during warm intervals by
the sapropel records  \citep{Toucanneetal2015}. 

Thus, it is expected that high-frequency Heinrich events induced rapid
climatic changes in the Mediterranean region with a succession of dry
and cold events followed by rapid warming and moisture return 
\citep{Toucanneetal2015}. Lacustrine sediments in eastern Albania also
recorded HEs-induced climatic changes through proxies of the
alteration, like a high concentration of manganese and total inorganic
carbon  \citep{Wagneretal2010} and a high zirconium/titanium ratio 
\citep{Wagneretal2009}.

\subsection{Geology and rivers of Albania}\label{sec3.2}  
The Albanian mountains are parts of the fold belt, which was thrusted
westward during the subduction of the Adriatic plate beneath
southeastern Europe  \citep{Roureetal2004}. The eastern side of
Albanides mainly consists of Jurassic ophiolites and Mesozoic
carbonates. The western side of Albanides is mainly formed of
carbonates topped by Mesozoic or Cenozoic flysch deposits 
\citep{RobertsonShallo2000}. A foreland basin, filled with
Plio-Quaternary molasse deposits, forms the coastal plain 
\citep{Roureetal2004}. 

The late Pleistocene uplift rate, inferred from fluvial incision,
locally reaches 2.8~mm/yr in the Albanian mountain but is generally in
the range 0.5 to 1.0~mm/yr 
\citep{Carcailletetal2009,Guzmanetal2013,Biermannsetal2018}. Permanent
GPS stations indicate the same range of values for the present-day
vertical motion in Albania (Jouanne, personal communication).

The main Albanian rivers are, from south to north, the Vjosa, Osum,
Devoll, Shkumbin, Erzen, Mat and Drin rivers  (Figure~\ref{fig1}) and
all of them are less than 272~km long.

Fluvial terrace deposition punctuates the vertical incision along all
the main Albanian  rivers (Figure~\ref{fig2}) and most of them are
located above soft clastic (flysch or molasses) sediments. The terraces
of the upper Vjosa River (also called Voidomatis in Greece), the middle
Vjosa River, the Osum River, the Erzen River and the Drin River were
previously mapped and dated by  \citet{Woodwardetal2008}, 
\citet{Haueretal2021},  \citet{Carcailletetal2009}, \citet{Koci2007}
and by  \citet{Gemignanietal2022}, respectively. We performed an
analysis of the terrace geometry and new dating for the Devoll,
Skumbin, Mat and Erzen rivers, previously poorly studied. The lower
part of the Drin River has not been studied because it is drowned by
several artificial dams.

\section{Terrace geomorphology and ages along the seven Albanian
rivers}\label{sec4}  
A synthesis of the numerical dating and terrace geometry is presented
for the rivers of Albania and northwestern Greece. A nomenclature is
proposed, where the successions of terraces surface for each river are
called Tx$_{(\mathrm{river})}$ and terrace indices increase with age.
Units are nonetheless labelled Ux$_{(\mathrm{river})}$ when the terrace
surface, fully eroded, cannot be defined.  A correlation of this
nomenclature with those used by the previous terrace studies is shown
in\unskip\break 
Table~\ref{tab3} and detailed in Supplementary Information,
Appendix~3.  

\begin{sidewaystable*}
\vspone
\caption{\label{tab3}Correlation of the local terrace nomenclatures
with a regional nomenclature for the terraces identified along the
Albanian rivers}
\begin{tabular}{c}
\tbody
\inlinefig{fx01}
\end{tabular}
\tabnote{The light green cells refer to dated levels; light
yellow and white cells refer to not dated levels, well correlated or
poorly correlated, respectively. The colored cells on the right side
refer to the color code  of Figures~\ref{fig3}, \ref{fig5},  \ref{fig7}
and~\ref{fig9}.  The regional ages of the terrace and their
uncertainties (68\% probability interval) are obtained from the
probability density curves of the numerical dating for terraces younger
than 60~ka (see text  and Figure~\ref{fig9}). ``P \& M'' stands for 
\citet{PriftiMecaj1987} and ``G and al.'' stands for 
\citet{Guzmanetal2013}.}
\end{sidewaystable*}

\subsection{Previous studies of the Vjosa, Drin and Osum river
terraces}\label{sec4.1} 
The Vjosa River is more than 272~km long and is made up of sections
with very different morphologies  \citep{Haueretal2021}.

In the upper section (Konista area,  Figure~\ref{fig1}), eight units 
(Figure~\ref{fig4}a), including the present-day channel
(T1$_{(\mathrm{vj})}$), were identified. They were dated, except
T2$_{(\mathrm{vj})}$, using different methods ($\mbox{}^{14}$C, U/Th,
ESR, TL) 
\citep{Lewinetal1991,Hamlinetal2000,Woodwardetal2001,Woodwardetal2008}
(Table~\ref{tab2}). The highest terrace was deposited by a river system
with a much larger catchment that was pirated before 350~ka 
\citep{Macklinetal1997}.

In the middle section of the Vjosa River, the long-term incision rate
is greater than in the upper section  \citep{Guzmanetal2013}. The
elevation of the highest terrace T10$_{(\mathrm{vj})}$ 
(Figure~\ref{fig3}a) is more than 160~m  \citep{Prifti1981} and our
field work has shown that the conglomerate unit of
T10$_{(\mathrm{vj})}$ is preserved between paleo-meanders filled by
sediment of T9$_{(\mathrm{vj})}$.  \citet{PriftiMecaj1987} mapped five
terrace levels and  \citet{Guzmanetal2013} mapped another terrace level
T2$_{(\mathrm{vj})}$ that is located at the top of a thick sedimentary
unit that extends several tens of meters below the present river 
\citep{Prifti1981}. 

The units beneath the terrace surfaces are mainly formed of rounded
fluvial clasts. Nonetheless, angular calcareous clasts are locally
intercalated within the fluvial units and are related to debris flows 
(Figure~\ref{fig3}b) provided by very steep calcareous slopes. 
\citet{Guzmanetal2013} dated colluvium above the top of
T2$_{(\mathrm{vj})}$.

We dated in this paper T5$_{(\mathrm{vj})}$ with an age intercalated
between those found in the upper section for T4$_{(\mathrm{vj})}$ and
T6$_{(\mathrm{vj})}$  \citep{Woodwardetal2008}. Hence, when the upper
and middle sections of the Vjosa River are considered, ten river
terrace levels are identified and only T9$_{(\mathrm{vj})}$ is not
dated  (Figure~\ref{fig3}a,  Table~\ref{tab2}). 

Along the Drin River, four terraces are described
\citep{Aliajetal1996,PashkoAliaj2020}. 
Our personal work close to
Peshkopia area  (Figure~\ref{fig1}) has revealed two others higher
terraces, T5$_{(\mathrm{dr})}$ and T6$_{(\mathrm{dr})}$ 
(Figure~\ref{fig3}f). Only T2$_{(\mathrm{dr})}$ and
T3$_{(\mathrm{dr})}$ terraces were dated  \citep{Gemignanietal2022}
(Table~\ref{tab2}). 

In the Osum River area, nine terraces were mapped 
\citep{Carcailletetal2009} and our complementary observations indicate
remnants of a fill\unskip\break 
terrace (T10$_{(\mathrm{os})}$) more than 150 m
above the present-day river  (Figure~\ref{fig3}b). The sedimentary unit
linked to T4$_{(\mathrm{os})}$ is superimposed above another
allostatigraphic unit U5$_{(\mathrm{os})}$ in the middle reaches of the
Osum River  \citep{Carcailletetal2009}. Using $\mbox{}^{14}$C and
$\mbox{}^{10}$Be dating methods,  \citet{Carcailletetal2009} dated
T7$_{(\mathrm{os})}$, T6$_{(\mathrm{os})}$, T3$_{(\mathrm{os})}$, and
T2$_{(\mathrm{os})}$ and also U5$_{(\mathrm{os})}$ 
(Table~\ref{tab2}).\looseness=-1

\begin{figure*}
\includegraphics{fig03}
\bcaption{\label{fig3}}{2}{\fontsize{9.7}{12}\selectfont
Ages and simplified geometry of the terraces
identified along the 7 main Albanian rivers (a--f; see text). The
horizontal and vertical axes are not to scale. The local terrace
nomenclature TX$_{(\mathrm{loc})}$ is indicated for each river. The
color of the terraces indicates the inferred correlation with the
regional nomenclature T0 to T12 (Same colors as cells of
Table~\ref{tab3}). The ages refer to the numerical ages of
Table~\ref{tab2}. Ages are shown as a unique interval with an ``*'' if
there are three or more numeric dates for one terrace level.} 
\vspace*{-3pt}
\end{figure*}

\subsection{New results about the paleo-Devoll, Mat and Erzen
terraces}\label{sec4.2} 

\subsubsection{A paleo-Devoll River defined from the Devoll and
Shkumbin terraces}\label{sec4.2.1} 
The Devoll River flows over 205~km. Downstream from the confluence with
the Osum River, it forms the Seman River  (Figure~\ref{fig5}a). 

The Shkumbin River is 181 km long and the Devoll and Shkumbin are two
nearby rivers that are presently separated by the C\"{e}rrik plain
spanning approximately  20~km$^{2}$. Today, no river flows through this
plain  (Figure~\ref{fig5}a) that dips ${\sim}0.1\text{\textdegree}$
toward the northwest but terraces of a paleo-river are perched above
its eastern border. The C\"{e}rrik plain is located over a thick
sedimentary unit  \citep{PriftiMecaj1987} and the scarp cut by the
Devoll River shows a ${>}$12~m-thick deposit formed of pebbles
supported by a sandy to silty matrix. Our measurements of imbricate
clasts and cross stratification indicate paleo-flow directions around N
300\textdegree\ and N 340\textdegree\ during deposition (site 1 and 2
on  Figure~\ref{fig4}c and  Supplementary Information, 
Appendix~4). This
suggests that the paleo-Devoll River flowed northward and connected to
the Shkumbin River. Hence, the terraces located along the middle
reaches of the Devoll and the lower reaches of the Shkumbin form a
unique terrace system that extends more than 100~km. 

\begin{figure}
\vspace*{3pt}
\includegraphics{fig04}
\vspace*{6pt}
\caption{\label{fig4}Evolution of the connections between the Devoll,
Osum, Seman and Shkumbin rivers. (a)~Present-day configuration.
(b)~Previous configurations. The age of the capture of the Devoll by
the Seman is estimated at 6 ka (see text). The paleo-Seman River from 
\citet[][full line]{Chabreyrou2006} and
\citet[][dashed lines]{Fouacheetal2010}.
(c)~Rose diagrams of the paleo-flow directions inferred from
imbricate clasts and cross stratification. Location of sites 1 and 2 on
Figure~\ref{fig4}b (data in the Supplementary Information, 
Appendix~4).}
\end{figure}

Four and six terrace levels were initially identified along the
Shkumbin \citep{Melo1961} and Devoll  \citep{Prifti1984} rivers,
respectively. In this study (Supplementary Information, 
Appendix~5), we
mapped and correlated eleven terrace levels 
along the paleo-Devoll
River  (Table~\ref{tab3} and  Figure~\ref{fig3}c). Their sedimentary
units were generally deposited on straths beveled in the flysch or
molasse substratum.

\begin{figure*}
\includegraphics{fig05}
\caption{\label{fig5}The terraces of the upper reaches of the Devoll
River. (a)~Panoramic view and (b)~cross-section through the terraces.
The ages refer to the regional nomenclature and to the most likely age
of abandonment proposed in this study (Table~\ref{tab3}).}
\end{figure*}

The mean thickness of T12$_{(\mathrm{pa})}$, T11$_{(\mathrm{pa})}$,
T9$_{(\mathrm{pa})}$, T8$_{(\mathrm{pa})}$, T7$_{(\mathrm{pa})}$,
pT6$_{(\mathrm{pa})}$, and T5$_{(\mathrm{pa})}$, T4$_{(\mathrm{pa})}$
and T3$_{(\mathrm{pa})}$ vary between 6 and 32~m and two superposed
sub-units, that are part
of parts of the same fluvial\unskip\break 
process, are
found beneath all these terraces: A thin upper sedimentary sub-unit
(${\sim}$1~m) is composed of clay, siltstone and fine sand.
Nevertheless, its thickness reaches more than 2 m beneath the oldest
terraces (T12$_{(\mathrm{pa})}$, T11$_{(\mathrm{pa})}$ and
T9$_{(\mathrm{pa})}$) and possibly includes loess and colluvium
deposited after the fluvial story. The basal sub-unit consists of
rounded pebbles and cobbles that are supported by a gravel and sand
matrix. The clast size generally fines upward, while the percentage of
matrix increases. Nonetheless, the size of the coarse material shows
complex variations and conglomerate sometimes alternate with horizontal
stratified, fine to coarse sand levels. Sediments of the basal unit
were deposited in a braided alluvial system characterized by
cross-stratified rounded pebbles and cobble levels that alternate with
horizontal stratified, fine to coarse sand levels.

The upper part of T10$_{(\mathrm{pa})}$ is fully eroded and
U10$_{(\mathrm{pa})}$ is only found beneath an erosional surface in the
continuity of the strath at the bottom of T9$_{(\mathrm{pa})}$.
Evidence of a meandering environment is found within the unit
U10$_{(\mathrm{pa})}$  (Figure~\ref{fig3}c) where sediments dip steeply
and were possibly deposited at the intrados of meanders. 

In the lower reaches of the paleo-Devoll catchment, a cosmogenic depth
profile  (Figure~\ref{fig8}a) yielded a minimum exposure age for
T3$_{(\mathrm{pa})}$ (Table~\ref{tab1}; see the description in 
Supplementary Information, 
Appendix~2) and seven $\mbox{}^{14}$C
samples were collected along the paleo-Devoll River 
(Table~\ref{tab2}). These results, combined with the eleven
$\mbox{}^{14}$C dates  \citep{Guzmanetal2013} gave ages for
T8$_{(\mathrm{pa})}$, T7$_{(\mathrm{pa})}$, T5$_{(\mathrm{pa})}$,
T4$_{(\mathrm{pa})}$, T3$_{(\mathrm{pa})}$, and T2$_{(\mathrm{pa})}$.
Furthermore, the $\mbox{}^{14}$C dating of colluvium deposited above
T1$_{(\mathrm{pa})}$ provides an age for the abandonment of this
terrace. 

\begin{figure*}
\includegraphics{fig06}
\caption{\label{fig6}The $\mbox{}^{10}$Be concentration along the depth
profiles. (a)~T3$_{(\mathrm{pa})}$ in the lower reaches of the paleo-Devoll
River (location of Sk-10  on the Supplementary Information,
Figure~S4a in Appendix~5); 
(b) T8$_{(\mathrm{ma})}$ in the middle reaches of the Mat River
(Ulza Dam, location on Figure~\ref{fig7}). Solid lines indicate the
best-fit for the depth-production profile; the dashed line shows the
inherited $\mbox{}^{10}$Be concentration. Details are given in
Table~\ref{tab1} and in the Supplementary Information, 
Appendix~2.} 
\end{figure*}

\begin{figure*}
\includegraphics{fig07}
\vspace*{3pt}
\caption{\label{fig7}Geomorphologic map of the Mat River. Location on
Figure~\ref{fig1}. The numbers refer to the samples of
Table~\ref{tab2}.}
\vspace*{6pt}
\end{figure*}

\subsubsection{Characteristics and numerical ages of the Mat
terraces}\label{sec4.2.2} 
Five terraces were previously described along the Mat River 
\citep{Melo1996}. Nine terraces  (Figure~\ref{fig3}e) were mapped
during our fieldwork (Figure~\ref{fig7}). 

\begin{figure}
\includegraphics{fig08}
\vspace*{3pt}
\caption{\label{fig8}Terraces of the Erzen River. 
(T3$_{(\mathrm{er})}$) extending toward the Tirana wind gap.}
\end{figure}

The two oldest terraces were dated using the $\mbox{}^{10}$Be method.
Amalgams of siliceous pebbles (e.g. radiolarites, chert, quartz), were
taken at the top of T9$_{(\mathrm{ma})}$ and T8$_{(\mathrm{ma})}$
(Ma-06 and Ma-04in  Table~\ref{tab1}; location on Figure~\ref{fig7}). A
cosmogenic depth profile was made through the sedimentary unit of
terrace T8$_{(\mathrm{ma})}$\unskip\break
(Figure~\ref{fig6}b). Terraces
T3$_{(\mathrm{ma})}$, T2$_{(\mathrm{ma})}$, T1$_{(\mathrm{ma})}$ and
the colluvium deposited above T1$_{(\mathrm{ma})}$ were dated from
charcoal samples (Table~\ref{tab2} and Figure~\ref{fig3}e).

\subsubsection{Characteristics and numerical ages of the Erzen
terraces}\label{sec4.2.3} 
The terraces of the Erzen River have been mapped by  \citet{Koci2007}
and an active back-thrust fault separates two domains 
\citep{Ganasetal2020}. In the western uplifted domain (Prespa
monocline), seven levels of terraces were recognized
(Figure~\ref{fig3}d) whereas in the eastern domain (Tirana syncline),
only three terrace levels were recognized. A correlation between the
terraces on each side of the back-thrust fault is made using the 15
$\mbox{}^{14}$C dates  (Table~\ref{tab2}) and seven terrace levels were
identified along the Erzen River (T7$_{(\mathrm{er})}$ to
T1$_{(\mathrm{er})}$), and only the oldest level is not numerically
dated. The terrace T3$_{(\mathrm{er})}$ is highly extended, in \mbox{peculiar}
across a wind gap  (Figure~\ref{fig8}), which corresponds to a paleo
river that flowed close to Tirana
(Figure~\ref{fig1}). \looseness=-1

\section{Discussion}\label{sec5} 

\subsection{A regional correlation of the Albanian terraces based on
numerical ages}\label{sec5.1} 
Few samples have been discarded during our work (Table~\ref{tab2}): two
$\mbox{}^{14}$C samples, that furnished less than 200-year ages in old
terraces, were considered as related to the reworking of recent organic
pieces. The Carbon quantity of five samples was too small (less than
0.12 mg) to give numerical ages. Two $\mbox{}^{10}$Be samples were also
excluded from the profile interpretations because one was probably
transported by a small tributary and the other one affected by a
probable chemical problem during the preparation (Supplementary
Information, 
Appendix~2). Finally, two TL ages published by 
\citet{Lewinetal1991} were removed due to their very high uncertainty. 

Thirty-one out of the 49 local terrace levels (Tx$_{(\mathrm{river})}$,
Figure~\ref{fig4}) recognized along the seven rivers were dated,
providing a solid framework for a regional correlation (Tx) based on
the synchronicity of numerical ages. No simple relationship between
altitude and age is observed at the scale of Albania 
(Figure~\ref{fig9}a) due to the variable uplift rate in the Albanian
mountains  \citep{Guzmanetal2013}.

To consider the 60 numerical ages younger than 60~ka,  a regional
probability density curve was obtained from the summation of the
individual probability distribution ages  \citep{Ramsey2009}, a method
already used in terrace chronology studies 
\citep[e.g.][]{Meyeretal1995,WegmannPazzaglia2002,WegmannPazzaglia2009}. 
The summation (Figure~\ref{fig9}b) shows time periods where the
probability of sedimentation is null and ten high probability peaks.
These peaks define the ages of T0 to T8  (Table~\ref{tab3}, see details
of the correlation in Supplementary Information, 
Appendix~6).

\begin{figure*}
\includegraphics{fig09}
\bcaption{\label{fig9}}{8}{Compilation of the Albanian terrace ages for the
last 60~ka  (Table~\ref{tab2}) and comparison with climatic proxis.
(a)~Plot of individual ages and their two sigma (95\%) probability.
Each terrace is represented by a symbol, a contour color and a fill
color corresponding to the river, the dating method and the terrace
level (regional nomenclature), respectively. The horizontal axis is the
terrace age while the vertical axis is the height of the terrace above
the present-day river. (b)~The regional probability density curve
produced by summing the probability distribution of the individual
ages; (c)~The $\delta^{18}$O record from the GISP2 ice core 
\citep{Grootesetal1993}. (d)~The percentage of the cold-water
foraminifera N. pachyderma from the Iberian margin 
\citep{deAbreuetal2003}. (e)~The paleo-environmental record from Lake
Ohrid (Zirconium/Titanium ratio: Zi/Ti)  \citep{Wagneretal2009}; and
(f)~the paleo-environmental record from Lake Prespa (Manganese: Mn) 
\citep{Wagneretal2010}. The timings of the Heinrich events (H1 to H5a)
are taken from  \citet{Rashidetal2003} and  \citet{Hemming2004}. The
gray rectangles represent the Heinrich events as identified by the
authors of curves (d--f). MIS, LGM and YD stand for Marine Isotope
Stage  \citep{Cachoetal1999}, Last Glacial Maximum 
\citep{Clarketal2009} and Younger Dryas  \citep{Berger1990}, 
respectively.}
\vspace*{-4pt}
\end{figure*}

The ages greater than 60~ka are few in number and the regional T9 to
T12 levels are only defined by one or two ages. Eighteen terrace levels
are not numerically dated along the various rivers. Their intercalation
between dated levels provides a rather good
relative age (yellow cells
on  Table~\ref{tab3}) or their elevation relative to the dated terrace
levels only provides a poor relative chronology (white cells 
in\unskip\break  
Table~\ref{tab3}). 

\subsection{The influence of the paleoclimate on the genesis of
Albanian terraces}\label{sec5.2}  
The comparison of the Albanian terraces ages with climatic proxies 
\citep{Grootesetal1993,deAbreuetal2003,Wagneretal2009,Wagneretal2010}
is a rather difficult exercise given the uncertainties about the
terrace abandonment ages (more than one thousand years) and the
short-term fluctuations in the climatic records  [less than one
thousand years, \citealp{Ziemenetal2019}]. 
A robust criterion could be
based on models that link the timing of sedimentation and incision with
the temperature, hydrology and vegetation evolutions during a climatic
cycle  \citep{Bull1991}.

Cold periods in Albania are associated with less precipitation 
\citep{Kalleletal2000,Toucanneetal2015} and we consider the classic
model for these climatic contexts, where vertical incision is favored
by the increase of the transport capacity that occurs at the transition
from cold and dry conditions to warmer and more humid conditions 
\citep[e.g.][]{Fulleretal1998,BridglandWestaway2008}. This model has
been proposed to define the ``cold'' terraces in the lowlands of
northern Europe  \citep{Vandenberghe2015}, to correlate terraces at the
Mediterranean scale  \citep{Macklinetal2002}, to interpret terraces in
semi-arid conditions  \citep{Vassalloetal2007} and to interpret the
nested terraces in Northern Apeninnes  \citep{WegmannPazzaglia2009} or
the western Carpathians  \citep{Olszak2017}. 

The succession of cold periods followed by rapid warm excursions, could
effectively cause the abandonment of most terraces 
(Figure~\ref{fig9}c): T2, T6 and T7 are synchronous with the end of the
Younger Dryas, the Dansgaard-Oeschger events number 7 and 11,
respectively 
\citep{Dansgaardetal1993,NorthGreenlandIceCoreProjectMembers2004}.
Furthermore, the abandonments of T8, T5, T4, and T3
(Figure~\ref{fig9}b) correlate rather well with the H5a 
\citep{Rashidetal2003}, H3, H2, and H1 Heinrich events
\citep{Hemming2004}, respectively  (Figure~\ref{fig9}c). These Heinrich
events were already recorded in this area 
\citep{Wagneretal2009,Wagneretal2010} (gray rectangle on
Figure~\ref{fig9}d--f). 

The ranges of the terrace ages, defined by the 95\% probability
interval of the summation curve, 
therefore include the ages of
transitions between cold-dry and warm-wet periods. Nonetheless, as the
climatic transitions were dated more precisely than the Albanian
terraces (less than a thousand years vs. more than a thousand years),
our results do not prove the ``cold'' terrace model of 
\citet{Vandenberghe2008} and are only in agreement with this model of
terrace genesis.

However, while rapid changes during the glacial cycle, such as DO or HE
events, can induce the formation of  ``cold'' terraces, the major
changes that occur between the glacial and interglacial periods are not
generally considered in this model. This is the case of T1 that is not
synchronous with a cold to warm transition.  \citet{Vandenberghe2008}
suggests that, in addition to the ``cold'' terrace model, deep channels
may be very rapidly incised and then filled at the beginning of a warm
period. This results in a ``warm'' unit model \citep{Vandenberghe2008}
and situations of rivers leaving their valley to take another course 
\citep{Vandenberghe1993} frequently typify ``warm'' units 
\citep{Vandenberghe2015}. 

T1 is related to the Holocene climatic optimum and a great aggradation
along the Vjoje (Figure~\ref{fig3}a) as well as deviations of the
rivers at the C\"{e}rrik and the Tirana wind gaps  (Figure~\ref{fig4}
and  Figure~\ref{fig8}) were recorded during this period. The T1
terrace would therefore be in line with the ``warm'' unit model 
\citep{Vandenberghe2015}. Similarly, the U10$_{(\mathrm{pa})}$, remnant
of a valley fill older than the T10 (90--117~ka) overlying unit, may
have been deposited during the Eemian interglacial (MIS-5e) stage and
could be a  ``warm'' sedimentary unit  \citep{Vandenberghe2015}.

\section{Conclusions}\label{sec6}  
Geomorphologic studies and new dating have been performed along the
Devoll, Shkumbin, Mat and Erzen rivers of Albania (30 $\mbox{}^{14}$C
sites, two $\mbox{}^{10}$Be profiles and two $\mbox{}^{10}$Be surface
sites). A comparison is also made with previous studies along the
Vjosa, Osum and Drin rivers. This work has led to a database of 70 ages
and a time correlation has been performed between the flights of
terraces observed along the seven rivers. It appears that 11 terrace
levels have been preserved during the last  200~ka in Albania and this
record contains most of the major phases of terrace formation in the
Mediterranean region during the last glacial cycle. The exceptional
preservation of the succession of Albanian terraces is probably due to
the combination of a moderate uplift rate (0.5 to 1 mm/year) and a
medium strength of the bedrock lithology (mainly flysch or molasse)
specific to this area. During the Holocene, T1 terrace level was
recognized, along with the capture of the Devoll River by the Osum
River and a tributary deviation away from the Erzen. Eight terraces (T2
to T10) were identified and dated during the last glacial period (MIS
5d to end of MIS 2). For the older periods, amongst the numerous
observed terrace remnants, only a unique of T11 was dated at
${\geq}194\pm19$~ka (MIS 6). 

The abandonment of the Albanian terrace surfaces was mainly controlled
by climatic variations and was generally synchronous with the
interstadial transitions during the last glacial period. This indicates
that the threshold necessary for a cold to warmer climatic control for
terrace development is reached during interstadial climatic events as
short as Heinrich events.

\section*{Declaration of interests}
The authors do not work for, advise, own shares in, or receive funds
from any organization that could \mbox{benefit} from this article, and have
declared no affiliations other than their research organizations.

\section*{Acknowledgements}
The authors would like to thank the NATO SFP 977993 and the Science for
Peace team for supporting this work. OG thanks the Simon Bolivar
University for granting him permission to carry out his doctoral
studies. This publication was also made possible through a grant
provided by the Institut de Recherche et Developement. We warmly thank
the staff of the AMS facility ASTER at the Centre Europ\'{e}en de
Recherche et d'Enseignement des G\'{e}osciences de l'Environnement
(CNRS, France) for technical assistance during the $\mbox{}^{10}$Be
measurements. We thank one anonymous reviewer and Johannes Preuss for
helpful comments. 

\back{}

\section*{Supplementary data}
Supporting information for this article is available on the journal's
website under \printDOI\ or from the author.  

\CDRsupplementaryTwotypes{supplementary-material}{\cdrattach{crgeos-251-suppl.pdf}}

\bibliographystyle{crgeos}
\bibliography{crgeos20230775}
\refinput{crgeos20230775-reference.tex}

\end{document}
